doi:10.1007/s00376-016-5241-9

Bui H. H., R. K. Smith, M. T. Montgomery, and J. Y. Peng, 2009: Balanced and unbalanced aspects of tropical cyclone intensification. Quart. J. Roy. Meteor. Soc., 135, 1715- 1731.10.1002/qj.502

4b945f82eeff3ee9a50772da5e1b7dc5

http%3A%2F%2Fonlinelibrary.wiley.com%2Fdoi%2F10.1002%2Fqj.502%2Fabstract

http://onlinelibrary.wiley.com/doi/10.1002/qj.502/abstractNot Available

Chan J. C. L., R. T. Williams, 1987: Analytical and numerical studies of the beta-effect in tropical cyclone motion. Part I: Zero mean flow. J. Atmos. Sci., 44, 1257- 1265.10.1175/1520-0469(1987)044<1257:AANSOT>2.0.CO;2

92a0d6677751d182bf80629bf2db502a

http%3A%2F%2Fadsabs.harvard.edu%2Fabs%2F1987JAtS...44.1257C

http://adsabs.harvard.edu/abs/1987JAtS...44.1257CNot Available

DeMaria M., 1985: Tropical cyclone motion in a nondivergent barotropic model. Mon. Wea. Rev., 113, 1199- 1210.10.1175/1520-0493(1985)1132.0.CO;2

5ad3186ab10b98f6ce240527abd6408c

http%3A%2F%2Fadsabs.harvard.edu%2Fabs%2F1985MWRv..113.1199D

http://adsabs.harvard.edu/abs/1985MWRv..113.1199DNot Available

DeMaria M., 1996: The effect of vertical shear on tropical cyclone intensity change. J. Atmos. Sci., 53, 2076- 2088.10.1175/1520-0469(1996)053<2076:TEOVSO>2.0.CO;2

d9c321b4b09313000cf962d4ba0509af

http%3A%2F%2Fadsabs.harvard.edu%2Fabs%2F1996JAtS...53.2076D

http://adsabs.harvard.edu/abs/1996JAtS...53.2076DCiteSeerX - Scientific documents that cite the following paper: The effect of vertical shear on tropical cyclone intensity change

DeMaria M., W. H. Schubert, 1984: Experiments with a spectral tropical cyclone model. J. Atmos. Sci., 41, 901- 924.10.1175/1520-0469(1984)041<0901:EWASTC>2.0.CO;2

7beb86b5-e3f7-4f22-b930-f57686e6dfac

847ea51179edcd6e79f6ae3c050a9095

http%3A%2F%2Fadsabs.harvard.edu%2Fabs%2F1984JAtS...41..901D

refpaperuri:(75944f094136f84866466af4b3010adf)

http://adsabs.harvard.edu/abs/1984JAtS...41..901DThe three-layer balanced axisymmetric tropical cyclone model presented by Ooyama (1969a) is generalized to three dimensions and the resultant primitive equations are solved using the Galerkin method with Fourier basis functions on a doubly-periodic mid-latitude (beta)-plane. The nonlinear terms are evaluated using the transform method where the necessary transforms are performed using FFT algorithms. The spectral equations are transformed so that the dependent variables represent the normal modes of the linearized equations. In this form, the application of nonlinear normal mode initialization is straightforward. The model is run with an axisymmetric initial condition of an f-plane and it is shown that many of the results presented by Ooyama (1969a) can be reproduced. The energy of the gravity and rotational modes are calculated and it is shown that the gravity mode energy is more than an order of magnitude smaller than the rotational mode energy. The model is then run on the (beta)-plane and it is shown that the tropical cyclone moves towards the northwest at about 2 ms('-1) and elongates towards the west and develops sharper geopotential gradients towards the east. The model is also run with a basic state wind profile and it is shown that large asymmetries develop. It is shown that the basic state wind in the upper layer can interact with the storm outflow to either increase or decrease the storm intensification rate, while the basic state in the lower layer can affect the intensification rate and the size of the model tropical cyclone. The effect of initialization procedures on a tropical cyclone forecast is also studied. The results from linear and nonlinear normal mode initialization and results from applying the nonlinear balance equation are compared. It is shown that the nonlinear normal mode initialization procedure results in much smaller track and intensity forecast errors, and prevents the excitation of spurious gravity waves. Several examples of tropical cyclone motion in the nondivergent barotropic model are presented. It is shown that the spectral truncation, horizontal diffusion coefficient and the tangential wind profile outside of the radius of maximum wind can each affect the track of a tropical cyclone in the barotropic model.

Dudhia J., 1989: Numerical study of convection observed during the winter monsoon experiment using a mesoscale two-dimensional model. J. Atmos. Sci., 46, 3077- 3107.10.1175/1520-0469(1989)0462.0.CO;2

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http://ci.nii.ac.jp/naid/10013124897Not Available

Ebita A., Coauthors, 2011: The Japanese 55-year reanalysis "JRA-55": An interim report. SOLA, 7, 149- 152.10.2151/sola.2011-038

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http%3A%2F%2Fci.nii.ac.jp%2Fnaid%2F130004940944%2F

http://ci.nii.ac.jp/naid/130004940944/The carbon monoxide (CO) dehydrogenase of Oligotropha carboxidovorans is composed of an S-selanylcysteine-containing 88. 7-kDa molybdoprotein (L), a 17.8-kDa iron-sulfur protein (S), and a 30.2-kDa flavoprotein (M) in a (LMS)(2) subunit structure. The flavoprotein could be removed from CO dehydrogenase by dissociation with sodium dodecylsulfate. The resulting M(LS)(2)- or (LS)(2)-structured CO dehydrogenase species could be reconstituted with the recombinant apoflavoprotein produced in Escherichia coli. The formation of the heterotrimeric complex composed of the apoflavoprotein, the molybdoprotein, and the iron-sulfur protein involves structural changes that translate into the conversion of the apoflavoprotein from non-FAD binding to FAD binding. Binding of FAD to the reconstituted deflavo (LMS)(2) species occurred with second-order kinetics (k(+1) = 1350 M(-1) s(-1)) and high affinity (K(d) = 1.0 x 10(-9) M). The structure of the resulting flavo (LMS)(2) species at a 2.8-A resolution established the same fold and binding of the flavoprotein as in wild-type CO dehydrogenase, whereas the S-selanylcysteine 388 in the active-site loop on the molybdoprotein was disordered. In addition, the structural changes related to heterotrimeric complex formation or FAD binding were transmitted to the iron-sulfur protein and could be monitored by EPR. The type II 2Fe:2S center was identified in the N-terminal domain and the type I center in the C-terminal domain of the iron-sulfur protein.

Emanuel K., C. DesAutels, C. Holloway, and R. Korty, 2004: Environmental control of tropical cyclone intensity. J. Atmos. Sci., 61, 843- 858.10.1175/1520-0469(2004)061<0843:ECOTCI>2.0.CO;2

e8cd2a868331337e39c36a6b2f8f5fc9

http%3A%2F%2Fadsabs.harvard.edu%2Fabs%2F2004JAtS...61..843E

http://adsabs.harvard.edu/abs/2004JAtS...61..843EThe influence of various environmental factors on tropical cyclone intensity is explored using a simple coupled ocean atmosphere model. It is first demonstrated that this model is capable of accurately replicating the intensity evolution of storms that move over oceans whose upper thermal structure is not far from monthly mean climatology and that are relatively unaffected by environmental wind shear. A parameterization of the effects of environmental wind shear is then developed and shown to work reasonably well in several cases for which the magnitude of the shear is relatively well known. When used for real-time forecasting guidance, the model is shown to perform better than other existing numerical models while being competitive with statistical methods. In the context of a limited number of case studies, the model is used to explore the sensitivity of storm intensity to its initialization and to a number of environmental factors, including potential intensity, storm track, wind shear, upper-ocean thermal structure, bathymetry, and land surface characteristics. All of these factors are shown to influence storm intensity, with their relative contributions varying greatly in space and time. It is argued that, in most cases, the greatest source of uncertainty in forecasts of storm intensity is uncertainty in forecast values of the environmental wind shear, the presence of which also reduces the inherent predictability of storm intensity.

Fang J., F. Q. Zhang, 2012: Effect of beta shear on simulated tropical cyclones. Mon. Wea. Rev., 140, 3327- 3346.10.1175/MWR-D-10-05021.1

1bdb43d2197ff9d6e5e82a440301fb1f

http%3A%2F%2Fadsabs.harvard.edu%2Fabs%2F2012MWRv..140.3327F

http://adsabs.harvard.edu/abs/2012MWRv..140.3327FThrough cloud-resolving simulations, this study examines the effect of 0205 on the evolution of tropical cyclones (TCs). It is found that the TC simulated on a 0205 plane with variable Coriolis parameter 04’ is weaker in intensity but larger in size and strength than the TC simulated on an 04’ plane with constant 04’. Such differences result mainly from the effect of the 0205 shear rather than from the variation of 04’ due to the latitudinal change of the TC position, as illustrated in a three-stage conceptual model developed herein. The first stage begins with the establishment of the 0205 shear and the emergence of asymmetries as the TC intensifies. The 0205 shear peaks in value during the second stage that subsequently leads to the formation of an extensive stratiform region outside of the primary eyewall. The evaporative cooling associated with the stratiform precipitation acts to sharpen the low-level equivalent potential temperature gradient into a frontlike zone outside of the eyewall region, which leads to the burst of convection outside of the primary eyewall. The third stage is characterized by a weakening 0205 shear and the corresponding TC vortex axisymmetrization and expansion. The convection on the inner edge of the stratiform region becomes more organized in the azimuthal direction and eventually causes the TC structure to evolve in a manner similar to the secondary eyewall formation and eyewall replacement usually observed in TCs. It is the active convect0102on outs0102de of the pr0102mary eyewall that contributes to a relatively weaker but larger TC on the 0205 plane than that on the 04’ plane.

Fiorino M., R. L. Elsberry, 1989: Some aspects of vortex structure related to tropical cyclone motion.J. Atmos. Sci., 46, 975- 990.fd8d4f6dda4fbc011d56ad81d1ffeb52

http%3A%2F%2Fadsabs.harvard.edu%2Fabs%2F1989jats...46..975f

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Ge X. Y., W. Xu, and S. W. Zhou, 2015: Sensitivity of tropical cyclone intensification to inner-core structure. Adv. Atmos. Sci.,32(10), 1407-1418, doi: 10.1007/s00376-015-4286-5.10.1007/s00376-015-4286-5

0a3574fcfa37f8d32db70298466d5a96

http%3A%2F%2Fwww.cnki.com.cn%2FArticle%2FCJFDTotal-DQJZ201510008.htm

http://d.wanfangdata.com.cn/Periodical/dqkxjz-e201510008In this study, the dependence of tropical cyclone (TC) development on the inner-core structure of the parent vortex is examined using a pair of idealized numerical simulations. It is found that the radial profile of inner-core relative vorticity may have a great impact on its subsequent development. For a system with a larger inner-core relative vorticity/inertial stability, the conversion ratio of the diabatic heating to kinetic energy is greater. Furthermore, the behavior of the convective vorticity eddies is likely modulated by the system-scale circulation. For a parent vortex with a relatively higher inner-core vorticity and larger negative radial vorticity gradient, convective eddy formation and radially inward propagation is promoted through vorticity segregation. This provides a greater potential for these small-scale convective cells to self-organize into a mesoscale inner-core structure in the TC. In turn, convectively induced diabatic heating that is close to the center, along with higher inertial stability, efficiently enhances system-scale secondary circulation. This study provides a solid basis for further research into how the initial structure of a TC influences storm dynamics and thermodynamics.

Hack J. J., W. H. Schubert, 1986: Nonlinear response of atmospheric vortices to heating by organized cumulus convection. J. Atmos. Sci., 43, 1559- 1573.89a46b81ed18ddc23d3c49d27845f920

http%3A%2F%2Fadsabs.harvard.edu%2Fabs%2F1986jats...43.1559h

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Holland, G. J., 1983: Tropical cyclone motion: Environmental interaction plus a beta effect. J. Atmos. Sci., 40, 328- 342.10.1175/1520-0469(1983)040<0328:TCMEIP>2.0.CO;2

aaa135dbb3ac71426e4d7dbc54651782

http%3A%2F%2Fadsabs.harvard.edu%2Fabs%2F1983JAtS...40..328H

http://adsabs.harvard.edu/abs/1983JAtS...40..328HThe dynamics of tropical cyclone motion are investigated by solving the vergent barotropic vorticity equation on a beta plane. Two methods of solution are presented: a direct analytic solution for a constant basic current, and a simple numerical solution for a more general condition. These solutions indicate that cyclone motion can be accurately prescribed by a non linear combination of two processes: an interaction between the cyclone and its basic current (the well known steering concept), and an interaction with the earth's vorticity field which causes a westward deviation from the pure steering flow. The nonlinear manner in which these two processes combine together with the effect of asymmetries in the steering current raise some interesting questions on the way in which cyclones of different characteristics interact with their environment, and has implications for tropical cyclone forecasting and the manner in which forecasting techniques are derived. (Author)*TROPICAL CYCLONES

Hong S.-Y., J. Dudhia, and S.-H. Chen, 2004: A revised approach to ice microphysical processes for the bulk parameterization of clouds and precipitation. Mon. Wea. Rev., 132, 103- 120.10.1175/1520-0493(2004)1322.0.CO;2

7913d9ed85b1a9bbcdcb88db96a17cbb

http%3A%2F%2Fadsabs.harvard.edu%2Fabs%2F2004MWRv..132..103H

http://adsabs.harvard.edu/abs/2004MWRv..132..103HNot Available

Huang Y.-H., M. T. Montgomery, and C.-C. Wu, 2012: Concentric eyewall formation in Typhoon Sinlaku (2008). Part II: Axisymmetric dynamical processes. J. Atmos. Sci., 69, 662- 674.9f9fbbd87ad9075a02f2f76fdd45ed64

http%3A%2F%2Fonlinelibrary.wiley.com%2Fresolve%2Freference%2FXREF%3Fid%3D10.1175%2FJAS-D-11-0114.1

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Li T., X. Y. Ge, M. Peng, and W. Wang, 2012: Dependence of tropical cyclone intensification on the Coriolis parameter. Tropical Cyclone Research and Review, 1, 242- 253.857b513b44111f4633eb39b479bb6439

http%3A%2F%2Fwww.researchgate.net%2Fpublication%2F271217113_Dependence_of_tropical_cyclone_intensification_on_the_Coriolis_parameter

http://www.researchgate.net/publication/271217113_Dependence_of_tropical_cyclone_intensification_on_the_Coriolis_parameter

Madala R. V., S. A. Piacsek, 1975: Numerical simulation of asymmetric hurricanes on a 尾-plane with vertical shear. Tellus, 27, 453- 468.10.1111/j.2153-3490.1975.tb01699.x

2a2cc7e9-e538-4b2e-8022-d8fc0590cdee

2b4144ad26e593a9ff9694bbaebfef93

http%3A%2F%2Fonlinelibrary.wiley.com%2Fdoi%2F10.1111%2Fj.2153-3490.1975.tb01699.x%2Fpdf

refpaperuri:(da9f8458afbe4d845c693d784a852783)

http://onlinelibrary.wiley.com/doi/10.1111/j.2153-3490.1975.tb01699.x/pdfAbstract A three-layer, semi-implicit model was developed to simulate moving and asymmetric hurricanes on a β-plane, using Kuo's method of cumulus parametrization. Sensible and latent heat transfer from ocean to atmosphere was included implicitly in the model. In order to predict hurricane movement over a large area and yet resolve finer details near the eye, a multi-grid network was used with a movable finest grid of 20 km mesh size, surrounded by two coarse grid nets with mesh spacings of 60 km and 180 km, respectively. A comparison of the results with f -plane calculations shows that the vortex on the β-plane intensified at a slower rate before the storm stage, but at the same rate thereafter. The β-plane hurricane was asymmetric throughout its life cycle, and these asymmetrics looked similar to those observed in real hurricanes. The vortex moved on the β-plane with a phase velocity of 4.3 km hour 611 for the westerly and 3.3 km hour 611 for the northerly components. The model was also integrated for two cases where the initial vortex was superimposed on a vertically varying basic current. Results showed that the strength of the simulated hurricane depends very much upon the magnitude of the vertical shear of the basic current; for a large shear (≥ 15 m sec 611 /12 km) the vortex failed to intensify into a hurricane. Computations showed that the pressure weighted mean of the basic current between the surface and 12 km level agreed very well with the magnitude of the steering current. As a result of the interaction between the hurricane circulation and the basic current, the hurricane moved in an oscillatory path with an amplitude of 30 km and a period of about 20 hours.

Mlawer E. J., S. J. Taubman, P. D. Brown, M. J. Iacono, and S. A. Clough, 1997: Radiative transfer for inhomogeneous atmospheres: RRTM, a validated correlated-k model for the longwave. J. Geophys. Res., 102, 16 663- 16 682.10.1029/97JD00237

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bf5f762e845a497b1ec8058223fb6df8

http%3A%2F%2Fonlinelibrary.wiley.com%2Fdoi%2F10.1029%2F97JD00237%2Fpdf

refpaperuri:(98daaed043b544401196cd274fa354f5)

http://onlinelibrary.wiley.com/doi/10.1029/97JD00237/pdfA rapid and accurate radiative transfer model (RRTM) for climate applications has been developed and the results extensively evaluated. The current version of RRTM calculates fluxes and cooling rates for the longwave spectral region (10-3000 cm) for an arbitrary clear atmosphere. The molecular species treated in the model are water vapor, carbon dioxide, ozone, methane, nitrous oxide, and the common halocarbons. The radiative transfer in RRTM is performed using the correlated-k method: the k distributions are attained directly from the LBLRTM line-by-line model, which connects the absorption coefficients used by RRTM to high-resolution radiance validations done with observations. Refined methods have been developed for treating bands containing gases with overlapping absorption, for the determination of values of the Planck function appropriate for use in the correlated-k approach, and for the inclusion of minor absorbing species in a band. The flux and cooling rate results of RRTM are linked to measurement through the use of LBLRTM, which has been substantially validated with observations. Validations of RRTM using LBLRTM have been performed for the midlatitude summer, tropical, midlatitude winter, subarctic winter, and four atmospheres from the Spectral Radiance Experiment campaign. On the basis of these validations the longwave accuracy of RRTM for any atmosphere is as follows: 0.6 W m(relative to LBLRTM) for net flux in each band at all altitudes, with a total (10-3000 cm) error of less than 1.0 W mat any altitude; 0.07 K dfor total cooling rate error in the troposphere and lower stratosphere, and 0.75 K din the upper stratosphere and above. Other comparisons have been performed on RRTM using LBLRTM to gauge its sensitivity to changes in the abundance of specific species, including the halocarbons and carbon dioxide. The radiative forcing due to doubling the concentration of carbon dioxide is attained with an accuracy of 0.24 W m, an error of less than 5%. The speed of execution of RRTM compares favorably with that of other rapid radiation models, indicating that the model is suitable for use in general circulation models.

Noh Y., W. G. Cheon, S. Y. Hong, and S. Raasch, 2003: Improvement of the K-profile model for the planetary boundary layer based on large eddy simulation data. Bound.-Layer Meteor., 107, 401- 427.10.1023/A:1022146015946

ebfc6da0-44fb-434f-9c8b-7b341d91258f

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http%3A%2F%2Fwww.springerlink.com%2Fcontent%2Fm7847n667m47v41w%2F

refpaperuri:(18193937665365080c4f347114f8bfc9)

http://www.springerlink.com/content/m7847n667m47v41w/Modifications of the widely used K-profile model of the planetary boundary layer (PBL), reported by Troen and Mahrt (TM) in 1986, are proposed and their effects examined by comparison with large eddy simulation (LES) data. The modifications involve three parts. First, the heat flux from the entrainment at the inversion layer is incorporated into the heat and momentum profiles, and it is used to predict the growth of the PBL directly. Second, profiles of the velocity scale and the Prandtl number in the PBL are proposed, in contrast to the constant values used in the TM model. Finally, non-local mixing of momentum was included. The results from the new PBL model and the original TM model are compared with LES data. The TM model was found to give too high PBL heights in the PBL with strong shear, and too low heights for the convection-dominated PBL, which causes unrealistic heat flux profiles. The new PBL model improves the predictability of the PBL height and produces profiles that are more realistic. Moreover, the new PBL model produces more realistic profiles of potential temperature and velocity. We also investigated how each of these three modifications affects the results, and found that explicit representation of the entrainment rate is the most critical.

Peng M. S., B.-F. Jeng, and R. T. Williams, 1999: A numerical study on tropical cyclone intensification. Part I: Beta effect and mean flow effect. J. Atmos. Sci., 56, 1404- 1423.10.1175/1520-0469(1999)056<1404:ANSOTC>2.0.CO;2

2cc173dc96db276af8552dd2243ec987

http%3A%2F%2Fadsabs.harvard.edu%2Fabs%2F1999JAtS...56.1404P

http://adsabs.harvard.edu/abs/1999JAtS...56.1404PThe effect of planetary vorticity gradient (beta) and the presence of a uniform mean flow on the intensification of tropical cyclones are studied using a limited-area primitive equation model. The most intense storm evolves on a constant-f plane with zero-mean flow and its structure is symmetric with respect to the vortex center. The presence of an environmental flow induces an asymmetry in a vortex due to surface friction. When f varies the vortex is distorted by the beta gyres. Fourier analysis of the wind field shows that a deepening cyclone is associated with a small asymmetry in the low-level wavenumber-one wind field. A small degree of asymmetry in the wind field allows a more symmetric distribution of the surface fluxes and low-level moisture convergence. On the other hand, a weakening or nonintensifying cyclone is associated with a larger asymmetry in its wavenumber-one wind field. This flow pattern generates asymmetric moisture convergence and surface fluxes and a phase shift may exist between their maxima. The separation of the surface flux maximum and the lateral moisture convergence reduces precipitation and inhibits the development of the tropical cyclone. Since the orientation of the asymmetric circulation induced by beta is in the southeast to northwest direction, the asymmetry induced by a westerly flow partially cancels the beta effect asymmetry while that of an easterly flow enhances it. Therefore, in a variable-f environment, westerly flows are more favorable for tropical cyclone intensification than easterly flows of the same speed.

Powell M. D., 1990: Boundary layer structure and dynamics in outer hurricane rainbands. Part II: Downdraft modification and mixed layer recovery. Mon. Wea. Rev., 118, 918- 938.10.1175/1520-0493(1990)118<0918:BLSADI>2.0.CO;2

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http%3A%2F%2Fadsabs.harvard.edu%2Fabs%2F1990MWRv..118..918P

refpaperuri:(e04632faf93de8b371790b637bd58fdc)

http://adsabs.harvard.edu/abs/1990MWRv..118..918PNot Available

Rappaport, E. N., Coauthors, 2009: Advances and challenges at the National Hurricane Center. Wea.Forecasting, 24, 395- 419.10.1175/2008WAF2222128.1

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http%3A%2F%2Fadsabs.harvard.edu%2Fabs%2F2009WtFor..24..395R

http://adsabs.harvard.edu/abs/2009WtFor..24..395RNot Available

Schecter D. A., D. H. Dubin, 1999: Vortex motion driven by a background vorticity gradient. Phys. Rev. Lett., 83, 2191.10.1103/PhysRevLett.83.2191

7593a288bb667c502ec2dd22cc2c129a

http%3A%2F%2Fjournals.aps.org%2Fprl%2Fabstract%2F10.1103%2FPhysRevLett.83.2191

http://journals.aps.org/prl/abstract/10.1103/PhysRevLett.83.2191The motion of self-trapped vortices on a background vorticity gradient is examined numerically and analytically. The vortices act to level the local background vorticity gradient. Conservation of momentum dictates that positive vortices (“clumps”) and negative vortices (“holes”) react oppositely: clumps move up the gradient, whereas holes move down the gradient. A linear analysis gives the trajectory of small clumps and holes that rotate against the local shear. Prograde clumps and holes are always nonlinear, and move along the gradient at a slower rate. This rate vanishes when the background shear is sufficiently large.

Schubert W. H., J. J. Hack, 1982: Inertial stability and tropical cyclone development. J. Atmos. Sci., 39, 1687- 1697.366ee78577768dcd8a2284c049291b21

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Shapiro L. J., H. E. Willoughby, 1982: The response of balanced hurricanes to local sources of heat and momentum. J. Atmos. Sci., 39, 378- 394.d50ade92889a7e5b59e5c0d404874eb9

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Terwey W. D., M. T. Montgomery, 2008: Secondary eyewall formation in two idealized, full-physics modeled hurricanes. J. Geophys. Res., 113,D12112, doi: 10.1029/2007JD008897.10.1029/2007JD008897

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http%3A%2F%2Fonlinelibrary.wiley.com%2Fdoi%2F10.1029%2F2007JD008897%2Fabstract

http://onlinelibrary.wiley.com/doi/10.1029/2007JD008897/abstractPrevailing hypotheses for secondary eyewall formation are examined using data sets from two high-resolution mesoscale numerical model simulations of the long-time evolution of an idealized hurricane vortex in a quiescent tropical environment with constant background rotation. The modeled hurricanes each undergo a secondary eyewall cycle, casting doubt on a number of other authors' hypotheses for secondary eyewall formation due to idealizations present in the simulation formulations. A new hypothesis for secondary eyewall formation is proposed here and is shown to be supported by these high-resolution numerical simulations. The hypothesis requires the existence of a region with moderate horizontal strain deformation and a sufficient low-level radial potential vorticity gradient associated with the primary swirling flow, moist convective potential, and a wind-moisture feedback process at the air-sea interface to form the secondary eyewall. The crux of the formation process is the generation of a finite-amplitude lower-tropospheric cyclonic jet outside the primary eyewall with a jet width on the order of a local effective beta scale determined by the mean low-level radial potential vorticity gradient and the root-mean square eddy velocity. This jet is hypothesized to be generated by the anisotropic upscale cascade and axisymmetrization of convectively generated vorticity anomalies through horizontal shear turbulence and sheared vortex Rossby waves as well as by the convergence of system-scale cyclonic vorticity by the low-level radial inflow associated with the increased convection. Possible application to the problem of forecasting secondary eyewall events is briefly considered.

Wang Y. Q., 1995: An inverse balance equation in sigma coordinates for model initialization. Mon. Wea. Rev., 123, 482- 488.10.1175/1520-0493(1995)1232.0.CO;2

882ed6c5e98e4cfab4222d5cb02a5db8

http%3A%2F%2Fadsabs.harvard.edu%2Fabs%2F1995MWRv..123..482W

http://adsabs.harvard.edu/abs/1995MWRv..123..482WNot Available

Wang Y. Q., 2009: How do outer spiral rainbands affect tropical cyclone structure and intensity? J. Atmos. Sci., 66, 1250- 1273.10.1175/2008JAS2737.1

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cd8d5604045d66cacadd3ba570056c28

http%3A%2F%2Fadsabs.harvard.edu%2Fabs%2F2009JAtS...66.1250W

refpaperuri:(af255fedfc79687b9a5f772c703f2709)

http://adsabs.harvard.edu/abs/2009JAtS...66.1250WFrey MH, Payne DA.

Wang Y. Q., G. J. Holland, 1996a: The beta drift of baroclinic vortices. Part I: Adiabatic vortices. J. Atmos. Sci., 53, 411- 427.10.1175/1520-0469(1996)053<0411:TBDOBV>2.0.CO;2

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http%3A%2F%2Fadsabs.harvard.edu%2Fabs%2F1996JAtS...53..411W

refpaperuri:(2d61c8a3fd71c1625b4820cc0f2d98ea)

http://adsabs.harvard.edu/abs/1996JAtS...53..411WThe dynamics of the movement of an initially axisymmetric baroclinic vortex embedded in an environment at rest on a beta plane is investigated with a three-dimensional primitive equation model. The study focuses on the motion and evolution of an adiabatic vortex and especially the manner in which vertical coupling of a tilted vortex influences its motion. The authors find that the vortex movement is determined by both the asymmetric flow over the vortex core associated with beta gyres and the flow associated with vertical projection of the tilted potential vorticity anomaly. The effects of vortex tilt can be large and complex. The secondary divergent circulation is found to be associated with the development of potential temperature anomalies required to maintain a balanced state. The processes involved strongly depend on the vertical structure, size, and intensity of the vortex together with external parameters such as the earth rotation and static stability of the environment. As a result, simple relationships between vortex motion and the vertical mean relative angular momentum are not always applicable.

Wang Y. Q., G. J. Holland, 1996b: The beta drift of baroclinic vortices. Part II: Diabatic vortices. J. Atmos. Sci., 53, 3737- 3756.10.1175/1520-0469(1996)053<3737:TBDOBV>2.0.CO;2

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http%3A%2F%2Fadsabs.harvard.edu%2Fabs%2F1996JAtS...53.3737W

refpaperuri:(f0aab038279efab2d5b651eff076eb20)

http://adsabs.harvard.edu/abs/1996JAtS...53.3737WPart II. Focuses on the beta drift of baroclinic vortices. Emphasis on diabatic vortices; Use of a three-dimensional primitive equation model; Difference in the motion and evolution of diabatic and adiabatic votices.

Wu C.-C., K. A. Emanuel, 1993: Interaction of a baroclinic vortex with background shear: Application to hurricane movement. J. Atmos. Sci., 50, 62- 76.10.1175/1520-0469(1993)050<0062:IOABVW>2.0.CO;2

deae02c7807095faed4f50a778912beb

http%3A%2F%2Fadsabs.harvard.edu%2Fabs%2F1993JAtS...50...62W

http://adsabs.harvard.edu/abs/1993JAtS...50...62WABSTRACT Most extant studies of tropical cyclone movement consider a barotropic vortex on a plane. However, observations have shown that real tropical cyclones are strongly baroclinic, with broad anticyclones aloft. Also, the distribution of the large-scale potential vorticity gradient in the tropical atmosphere is very nonuniform. These properties may substantially influence the movement of such storms.Note that the anticyclone above a hurricane will interact with the lower hurricane vortex and induce storm motion. Such interaction can be caused by both the direct effect of ambient vertical shear and the effect of vertical variation of the background potential vorticity gradient. In this paper, an attempt to isolate the effect of background vertical shear is made. The hurricane is represented in a two-layer quasigeostrophic model as a point source of mass and zero potential vorticity air in the upper layer, collocated with a point cyclone in the lower layer. The model is integrated by the method of contour dynamics and contour surgery.The results show that Northern Hemisphere tropical cyclones should have a component of drift relative to the mean flow in a direction to the left of the background vertical shear. The effect of weak shear is also found to be at least as strong as the effect, and the effect is maximized by a certain optimal ambient shear. The behavior of the model is sensitive to the thickness ratio of the two layers and is less sensitive to the ratio of the vortices' horizontal scale to the radius of deformation. Storms with stronger negative potential vorticity anomalies tend to exhibit more vortex drift.

Wu L. G., B. Wang, 2000: A potential vorticity tendency diagnostic approach for tropical cyclone motion. Mon. Wea. Rev., 128, 1899- 1911.10.1175/1520-0493(2000)128<1899:APVTDA>2.0.CO;2

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http%3A%2F%2Fadsabs.harvard.edu%2Fabs%2F2000MWRv..128.1899W

refpaperuri:(4cfecb8bb923d194011f21f1937a6095)

http://adsabs.harvard.edu/abs/2000MWRv..128.1899WIn order to understand the roles of various physical processes in baroclinic tropical cyclone (TC) motion and the vertical coupling between the upper- and lower-level circulations, a new dynamical framework is advanced. A TC is treated as a positive potential vorticity (PV) anomaly from environmental flows, and its motion is linked to the positive PV tendency. It is shown that a baroclinic TC moves to the region where the azimuthal wavenumber one component of the PV tendency reaches a maximum, but does not necessarily follow the ventilation flow (the asymmetric flow over the TC center). The contributions of individual physical processes to TC motion are equivalent to their contributions to the wavenumber one PV component of the PV tendency. A PV tendency diagnostic approach is described based on this framework. This approach is evaluated with idealized numerical experiments using a realistic hurricane model. The approach is capable of estimating TC propagation with a suitable accuracy and determining fractional contributions of individual physical processes (horizontal and vertical advection, diabatic heating, and friction) to motion. Since the impact of the ventilation flow is also included as a part of the influence of horizontal PV advection, this dynamical framework is more general and particularly useful in understanding the physical mechanisms of baroclinic and diabatic TC motion.

Wu L. G., S. A. Braun, 2004: Effects of environmentally induced asymmetries on hurricane intensity: A numerical study. J. Atmos. Sci., 61, 3065- 3081.10.1175/JAS-3343.1

4ab519fb4a7f2ae4d674475b56d6e196

http%3A%2F%2Fadsabs.harvard.edu%2Fabs%2F2004JAtS...61.3065W

http://adsabs.harvard.edu/abs/2004JAtS...61.3065WThe influence of uniform large-scale flow, the beta effect, and vertical shear of the environmental flow on hurricane intensity is investigated in the context of the induced convective or potential vorticity asymmetries in the core region with a hydrostatic primitive equation hurricane model. In agreement with previous studies, imposition of one of these environmental effects weakens the simulated tropical cyclones. In response to the environmental influence, significant wavenumber-1 asymmetries develop. Asymmetric and symmetric tendencies of the mean radial and azimuthal winds and temperature associated with the environment-induced convective asymmetries are evaluated. The inhibiting effects of environmental influences are closely associated with the resulting eddy momentum fluxes, which tend to decelerate tangential and radial winds in the inflow and outflow layers. The corresponding changes in the symmetric circulation tend to counteract the deceleration effect. The net effect is a moderate weakening of the mean tangential and radial winds. The reduced radial wind can be viewed as an anomalous secondary radial circulation with inflow in the upper troposphere and outflow in the lower troposphere, weakening the mean secondary radial circulation.

Zhu T., D.-L. Zhang, 2006: The impact of the storm-induced SST cooling on hurricane intensity. Adv. Atmos. Sci. ,23, 14-22, doi:10.1007/s00376-006-0002-9.10.1007/s00376-006-0002-9

1267dc5780c303278f5f8c9e3bbac10e

http%3A%2F%2Fd.wanfangdata.com.cn%2FPeriodical_dqkxjz-e200601002.aspx

http://d.wanfangdata.com.cn/Periodical_dqkxjz-e200601002.aspxThe effects of storm-induced sea surface temperature (SST) cooling on hurricane intensity are investigated using a 5-day cloud-resolving simulation of Hurricane Bonnie (1998). Two sensitivity simulations are performed in which the storm-induced cooling is either ignored or shifted close to the modeled storm track. Results show marked sensitivity of the model-simulated storm intensity to the magnitude and relative position with respect to the hurricane track. It is shown that incorporation of the storm-induced cooling, with an average value of 1.3℃, causes a 25-hPa weakening of the hurricane, which is about 20hPa per 1℃ change in SST. Shifting the SST cooling close to the storm track generates the weakest storm,accounting for about 47% reduction in the storm intensity. It is found that the storm intensity changes are well correlated with the air-sea temperature difference. The results have important implications for the use of coupled hurricane-ocean models for numerical prediction of tropical cyclones.