Pith. sign in

REVIEW 4 major objections 5 minor 81 references

Characterizing the energetics of multi-scale asymmetries during tropical cyclone rapid intensity changes

T0 review · 4 major / 5 minor · reviewed 2026-08-14 · deepseek-v4-flash

Challenge this review Re-run · record.json Download PDF Read on arXiv ↗ Review JSON

Pith's one-line read Rapid hurricane intensity change is driven by eddy–eddy energy exchange, not the mean flow

desk verdict A well-executed first demonstration of wavenumber-resolved TC energetics, but the headline mechanism claim is generalized from a Phailin-only order-of-magnitude table and needs tempering before it becomes a robust conclusion. read the letter →

arxiv 1908.03618 v1 pith:L254XOTN submitted 2019-08-09 physics.ao-ph physics.flu-dyn

Saiprasanth Bhalachandran , D. R. Chavas , F. D. Marks Jr. , S. Dubey , A. Shreevastava , T. N. Krishnamurti This is my paper · ORCID
classification physics.ao-phphysics.flu-dyn
keywords tropicalcyclonerapidintensitychangewavenumberenergeticsscaleinteractionsbaroclinicenergyconversioncross-scalekinetictransferazimuthalasymmetriesaxisymmetrizationstorm-resolvingsimulation
verification ladder T0 review T1 audit T2 compute T3 formal

The pith

A machine-rendered reading of the paper's core claim, the machinery that carries it, and where it could break.

The reading

The paper argues that the usual way of attributing tropical cyclone intensity change to the exchange of kinetic energy between the azimuthally averaged vortex and all asymmetries lumped together misses the action. Decomposing the storm into azimuthal wavenumbers, the authors find for three simulated storms that rapid intensification and rapid weakening are governed by two scale-resolved pathways: the direct baroclinic conversion of available potential energy to kinetic energy at each wavenumber, and the cross-scale transfer of kinetic energy among eddies of different wavenumbers. The barotropic mean–eddy exchange that has been the focus of earlier work is two orders of magnitude smaller over all lifecycle phases considered. If this ranking holds, intensity-change diagnostics and the linearized models used to study them should be refocused on baroclinic and cross-scale terms.

What carries the argument

The central object is scale-interaction energetics in the azimuthal-wavenumber domain. Model fields are interpolated onto a storm-centered cylinder, Fourier-transformed in azimuth, and grouped into wavenumber 0 (the mean vortex), wavenumbers 1–2 (persistent vortex-scale asymmetries), and wavenumbers 3 and higher (transient sub-vortex-scale asymmetries). Budget equations track available potential energy generation, baroclinic conversion from available potential to kinetic energy at each scale, barotropic kinetic-energy exchange between the mean and eddy scales, and triad-based cross-scale kinetic-energy exchange among eddy wavenumbers. This decomposition is what allows the paper to display the relative sizes of the competing energy pathways.

What would settle it

Compute the same wavenumber-resolved energy budget for many storms with frictional dissipation included and test whether barotropic mean–eddy exchange stays at least two orders of magnitude below baroclinic and cross-scale terms during both rapid intensification and rapid weakening; one case where mean–eddy exchange is comparable would overturn the ranking.

Watch

Extended reading notes

Core claim

Contrary to the conventional wisdom summarized in the paper, the primary mechanism of axisymmetrization is the baroclinic conversion from available potential to kinetic energy operating directly at wavenumber 0, not the barotropic mean–eddy transaction. Likewise, the primary mechanism of convective aggregation and disaggregation is the cross-scale exchange of kinetic energy among eddies of different wavenumbers, not the direct mean–eddy exchange. The order-of-magnitude analysis shows baroclinic and cross-scale terms exceed barotropic mean–eddy exchanges by at least two orders of magnitude throughout the life cycles studied, and the energetics of the asymmetries are largely independent of the mean.

Load-bearing premise

The ranking of energy pathways is computed from one selected forecast cycle per storm, averaged over a 0–300 km radius and 0–20 km height, with frictional dissipation omitted, and is then generalized to all rapid intensity changes; if those magnitudes are not representative, the ordering could change.

Editorial extensions

If this is right

  • Intensity-change diagnosis and forecasting should place more weight on baroclinic APE-to-KE conversion and eddy–eddy cross-scale transfers than on the barotropic mean–eddy term.
  • Linearized models that only permit mean–eddy interactions, and Reynolds-averaged eddy-flux diagnostics, would misattribute the role of asymmetries in rapid intensity changes.
  • Upscale kinetic-energy transfer during rapid intensification and downscale transfer during rapid weakening offer candidate early-warning signatures.
  • Because the energetics of the asymmeteries are largely independent of the mean, a storm can spin up while eddy energy grows, or lose mean energy while eddy energy continues to grow, complicating single-term intensity metrics.

Reading between the lines

Editorial extensions of the paper, not claims the author makes directly.

  • If the ordering persists across many storms, forecast improvement may come less from refining the symmetric core and more from improving how models represent energy transfer across scales, including subgrid convection and diffusion.
  • The same wavenumber decomposition could be applied to ensemble forecasts: the spread of cross-scale transfer magnitudes across members might predict the timing and probability of rapid intensification better than mean-state spread alone.
  • The vortex-centered formulation sees environment–vortex exchange only indirectly; recasting the triad energetics in an environment-centered or Cartesian domain could quantify that exchange explicitly.
  • Observational testing may be possible using aircraft-derived azimuthal wind and thermodynamic composites, though sampling at high wavenumbers would be challenging.
Share X Bluesky LinkedIn Reddit HN

Signed reviews

No signed human review yet.

Editorial analysis

A structured set of objections, weighed in public.

Desk editor's note, referee report, and a circularity audit.

Referee Report

4 major / 5 minor

Summary. The paper introduces a wavenumber-resolved energetics framework, based on Saltzman (1957) and Krishnamurti et al. (2005), to characterize azimuthal asymmetries in tropical cyclones during rapid intensity changes. Using HWRF forecasts of Phailin (2013), Lehar (2013), and Harvey (2017), the authors compute APE generation, APE-to-KE conversion, barotropic mean-eddy KE exchange, and cross-scale eddy-eddy KE transfers at WN 0, WNs 1-2, and WNs >=3. They report that RI is associated with symmetric APE generation and upscale KE transfer, while RW is associated with asymmetric APE generation and downscale transfer. Their central mechanistic claim, stated in Section 5, is that the primary axisymmetrization mechanism is baroclinic conversion from APE to KE directly at WN 0, and the primary convective (dis)aggregation mechanism is cross-scale eddy-eddy KE exchange, not barotropic mean-eddy transactions. The paper also identifies potential early-warning indicators of RI based on these energy transfers.

Significance. If the central claim is correct, the paper would provide a genuinely useful multi-scale diagnostic framework and would shift attention away from barotropic mean-eddy energetics in TC intensity-change research. The framework itself is transparent, requires no fitted parameters, and extends a well-established formalism to a storm-centered cylindrical geometry; the case-study descriptions are detailed and the appendix gives the principal equations. However, the paper's most consequential assertion rests on evidence that is narrower than the claim: the order-of-magnitude ranking is shown for Phailin only, frictional dissipation is omitted from the computed budgets despite being present in the equations, and each storm is represented by a single selected HWRF forecast cycle. These limitations make the mechanistic conclusion plausible but not established.

major comments (4)
  1. [Section 4.6, Figure 11, and Section 5] The order-of-magnitude analysis that supports the headline claim is computed for TC Phailin only, as the text in Section 4.6 states ('over the course of the life-cycles of TC Phailin'), but Section 5 then generalizes to 'the cases studied here' and concludes that baroclinic and cross-scale exchanges dominate barotropic transactions 'throughout the life-cycle of the cases studied here.' No equivalent order-of-magnitude table or figure is shown for Lehar or Harvey. Because this ranking is the load-bearing evidence for the mechanism claim, the generalization is unsupported. The authors should either present the analogous analysis for Lehar and Harvey or explicitly restrict the mechanistic conclusion to Phailin.
  2. [Section 2 and Section 5] Only one HWRF forecast cycle per storm is analyzed, and the text states that these are the cycles that 'best captured the rapid intensity changes.' This selection makes it impossible to assess whether the computed energy pathways are robust features of RI/RW or artifacts of a single favorable forecast. Since the paper draws general conclusions about RI versus RW energetics from these three cycles, the representativeness of the chosen cycles is load-bearing. The authors should justify the selection quantitatively or add a sensitivity analysis using additional cycles or ensemble members; in the absence of that, the claims should be framed as case-study illustrations rather than general findings.
  3. [Equations (2)-(3), Sections 4.1 and 5] The energy budgets in Equations (2) and (3) include frictional dissipation terms, but the paper explicitly states that frictional effects are not resolved and, in Section 5, acknowledges that friction may be scale-dependent and asymmetric. Given that the barotropic mean-eddy transactions in Figure 11 are two to three orders of magnitude smaller than the baroclinic and cross-scale terms, uncomputed frictional terms could be comparable to or larger than the smallest retained terms. The central ranking could therefore change if friction were included. The authors should quantify the omitted friction or, at minimum, provide a scaling argument showing that it cannot alter the ordering of the terms.
  4. [Section 4.3, Figures 7-8] The claim that 'a consistent signature of KE transfer from eddy to mean (mean to eddy) during RI (RW)' is 'notable only between the mean and higher-WN eddies' appears to be based on Phailin alone: Figure 8, which shows the mean versus high-WN exchange during both RI and RW, is presented for Phailin only, while Figure 7 shows low-WN exchanges for Phailin, Harvey, and Lehar. If the high-WN result has not been verified for the other two storms, the consistency claim in Section 5 should be softened or supplemented with additional cases.
minor comments (5)
  1. [Section 2] The initialization time for Lehar is given as '00 hours, 26th November 20130'; the year contains a typo and should read 2013.
  2. [Section 1] The sentence 'it behooves us identify the magnitude and nature of the impact of asymmetries' is missing the word 'to': it should read 'behooves us to identify.'
  3. [Figure 11 and Section 4.6] The order-of-magnitude figure would be easier to interpret if the columns and rows were explicitly labeled in the caption, with units for the energy transaction rates and a statement of the domain over which the averaging is performed.
  4. [References] In the reference list, the name 'V onich' contains a spurious space and should be 'Vonich.'
  5. [Section 4] The phrase 'the tendency of tangential momentum' in Equation (1) is followed by an equation with a pressure-gradient eddy term that is not defined in the list following the equation; adding a one-line definition would improve readability.

Circularity Check

0 steps flagged · score 0.0 of 10

No significant circularity: the energetics are computed directly from HWRF output, the framework equations are re-derived in the appendix, and the acknowledged limitations affect generalizability rather than creating a definitional reduction.

full rationale

I walked the paper's derivation chain: HWRF fields are projected onto a storm-centered cylinder, Fourier-decomposed into wavenumbers, and substituted into the spectral energy budgets of Eqs. 2-3, whose full forms are given in the appendix (Eqs. 4-17). Each term is evaluated from model output; no term is fitted to a target quantity, and no prediction is made from a parameter that was calibrated on the same quantity. The citation to Krishnamurti et al. (2005) supplies the cylindrical-coordinate scale-interaction formalism, but the paper reprints the equations in its appendix and credits Saltzman (1957) as the foundation, so the argument does not reduce to an unverified self-citation chain. The 'early-warning indicators' are presented as potential, in-sample signatures with explicit future-work plans for statistical testing on a larger set of cases, not as verified out-of-sample predictions. The limitations that are explicitly acknowledged, namely the Phailin-only order-of-magnitude table in Section 4.6, the single forecast cycle per storm, and the omission of explicit frictional dissipation, are scientific generalizability and budget-completeness concerns; they do not make any derived result equivalent to its input by construction. No circular step satisfying the quoted-evidence standard was found.

Assumptions & free parameters 3 free parameters · 4 assumptions · 0 invented entities

The paper introduces no new physical entities. It does introduce a free grouping of wavenumbers and methodological choices (center, volume bounds) that shape all quantitative comparisons. The principal assumptions are that the inherited scale-interaction equations are valid in this cylindrical formulation, that the three selected HWRF forecasts are representative, and that friction can be neglected without changing the ranking of terms.

free parameters (3)
  • Wavenumber grouping threshold
    WNs 1,2 are classified as persistent vortex-scale asymmetries and WNs 3 and above as transient sub-vortex-scale asymmetries. The cutoff is chosen by hand and the central findings depend on this grouping, though it is motivated by the 85% variance claim from Krishnamurti et al. (2005).
  • Storm center definition = surface-minimum pressure
    Chosen for the cylindrical coordinate transformation; the authors acknowledge in Section 2 that center choice can change low-wavenumber power, especially in sheared storms, and assert without demonstration that qualitative results are unaffected.
  • Domain averaging bounds = 0-300 km radius, 0-20 km height
    All domain-averaged energetics (Figures 5, 9-11) integrate over this volume; the order-of-magnitude comparison that drives the main claim depends on these bounds.
assumptions (4)
  • standard math Saltzman (1957) scale-interaction energy equations, as retailored to cylindrical TC coordinates by Krishnamurti et al. (2005), are correct and applicable.
    The entire diagnostic rests on Equations 2 and 3 and Appendix Equations 4 to 17; Equation (10) is introduced as 'can be shown to lead to' without a full derivation in this paper.
  • domain assumption The selected HWRF forecasts are representative of the real TCs' rapid intensity changes.
    Section 2 selects, for each storm, the single forecast cycle that 'best captured' the observed intensity change; the analysis conditions on good forecasts and does not test other cycles or model versions.
  • domain assumption Frictional dissipation is small enough that omitting it does not change the relative magnitude of the energy pathways or the conclusions about net KE change.
    Equations 2 and 3 include frictional terms F0 and Fn, but they are never computed; Section 5 states friction is out of scope, yet Figure 10 is presented as the net rate of change of KE.
  • standard math The Lorenz (1955) APE generation and baroclinic conversion definitions, including the static stability parameter gamma, apply to the model output.
    Equations 11 to 16 define APE generation and conversion as covariances of heating and temperature and of vertical velocity and temperature, standard in this literature.

how reviews work

0 comments
Cite this review

Pith. "Pith review of Characterizing the energetics of multi-scale asymmetries during tropical cyclone rapid intensity changes." pith.science (2026). https://pith.science/paper/L254XOTN

@misc{pith2026190803618,
  author       = {Pith},
  title        = {Pith review of: Characterizing the energetics of multi-scale asymmetries during tropical cyclone rapid intensity changes},
  year         = {2026},
  howpublished = {\url{https://pith.science/paper/L254XOTN}},
  note         = {Machine review of arXiv:1908.03618}
}
abstract

Our collective understanding of azimuthally-asymmetric features within the coherent structure of a tropical cyclone (TC) continues to improve with the availability of more detailed observations and high-resolution model outputs. However, a precise understanding of how these asymmetries impact TC intensity changes is lacking. Prior attempts at investigating the asymmetric impacts follow a mean-eddy partitioning that condenses the effect of all the asymmetries into one term and fails to highlight the differences in the role of asymmetries at different scales. In this study, we present a novel energetics-based approach to analyze the asymmetric impacts at multiple length-scales during periods of TC rapid intensity changes. Using model outputs of TCs under low and high shear, we compute the different energy pathways that enhance/suppress the growth of multi-scale asymmetries in the wavenumber (WN) domain. We then compare and contrast the energetics of the mean flow field (WN 0) with that of the persistent, coherent vortex-scale asymmetric structures (WNs 1,2) and the more local, transient, sub-vortex-scale asymmetries (WNs $\geq$ 3). We find in our case-studies that the dominant mechanisms of growth/decay of the asymmetries are the baroclinic conversion from available potential to kinetic energy at individual scales of asymmetries, and the transactions of kinetic energy between the asymmetries of various length-scales; rather than the barotropic mean-eddy transactions as is typically assumed. Our case-study analysis further shows that the growth/decay of asymmetries is largely independent of the mean. Certain aspects of eddy energetics can potentially serve as early-warning indicators of TC rapid intensity changes.

Figures

Figures reproduced from arXiv: 1908.03618 by the authors.

Figure 1
Figure 1. Time-series plot of intensity for (a) Phailin (initialized on 2013100912) (b) Lehar (initialized on [PITH_FULL_IMAGE:figures/full_fig_p023_1.png] view at source ↗
Figure 2
Figure 2. Radius-height plots of eddy radial vorticity flux for Phailin (Panel a; Time-averaged during the initial period [PITH_FULL_IMAGE:figures/full_fig_p024_2.png] view at source ↗
Figure 3
Figure 3. Lehar’s plan view (r-θ) plots of (a) eddy relative vorticity (shaded) and radial velocity (contours, black represents inflow and golden represents outflow) averaged between 6-10 km (mid-levels) in the vertical, 0 - 120 km radius and 24-36 hours (b) Same as (a) except that the shading represents eddy moist entropy (θe). Highlighted, are the regions where the inflow carries the positive eddy vorticity (a) and negative… view at source ↗
Figures from the paper (9 more)
Figure 4
Figure 4. Figure 4: (a,b) Plot of Phailin’s vertically integrated cloud-water mixing ratio ( [PITH_FULL_IMAGE:figures/full_fig_p025_4.png]
Figure 5
Figure 5. Figure 5: Time-series of the domain-averaged (up to a radius of 300 km, up to 20 km in the vertical) rate of change of [PITH_FULL_IMAGE:figures/full_fig_p026_5.png]
Figure 6
Figure 6. Figure 6: Phailin: Radius-height plots of the conversion from eddy potential to eddy kinetic energy for WNs 1,2 (a,c) [PITH_FULL_IMAGE:figures/full_fig_p027_6.png]
Figure 7
Figure 7. Figure 7: (Left) Radius-height plots of the barotropic exchange between the mean and low-WN asymmetries for TC [PITH_FULL_IMAGE:figures/full_fig_p028_7.png]
Figure 8
Figure 8. Figure 8: Radius-height plots of the barotropic exchange between the mean and WNs [PITH_FULL_IMAGE:figures/full_fig_p029_8.png]
Figure 9
Figure 9. Figure 9: (a) Time-series plot of Phailin’s (domain-averaged) rate of change of kinetic energy of low-wavenumbers [PITH_FULL_IMAGE:figures/full_fig_p030_9.png]
Figure 10
Figure 10. Figure 10: Time-series of the net change of KE in WNs 0,1,2,≥3 (blue, red, green and brown solid lines) in Phailin compared against the rate of change in intensity (black dashed line) over the course of its life-cycle. This figure serves to illustrate that due to the existence o…
Figure 11
Figure 11. Figure 11: Order of magnitude analysis for the various energy transactions over the course of TC Phailin’s life-cycle. [PITH_FULL_IMAGE:figures/full_fig_p032_11.png]
Figure 12
Figure 12. Figure 12: Summary of the insights from scale-interactions during RI and RW phases. In this figure, the weight of [PITH_FULL_IMAGE:figures/full_fig_p033_12.png]

Discussion (0). Continue with ORCID to comment.

Reference graph

Works this paper leans on

81 extracted references · 78 canonical work pages

  1. [1]

    , " * write output.state after.block = add.period write newline

    ENTRY address archive author booktitle chapter doi edition editor eid eprint howpublished department institution journal key month note number organization pages publisher school series title type url volume year label extra.label sort.label short.list INTEGERS output.state before.all mid.sentence after.sentence after.block FUNCTION init.state.consts #0 '...

  2. [2]

    write newline

    " write newline "" before.all 'output.state := FUNCTION if.digit duplicate "0" = swap duplicate "1" = swap duplicate "2" = swap duplicate "3" = swap duplicate "4" = swap duplicate "5" = swap duplicate "6" = swap duplicate "7" = swap duplicate "8" = swap "9" = or or or or or or or or or FUNCTION n.separate 't := "" #0 'numnames := t empty not t #-1 #1 subs...

  3. [3]

    Alaka, G. J., X. Zhang, S. G. Gopalakrishnan, S. B. Goldenberg, and F. D. Marks, 2017: Performance of basin-scale HWRF tropical cyclone track forecasts. Weather and Forecasting, 32 (3), 1253--1271

    work page 2017

  4. [4]

    A., 1972: Development of asymmetries in a three-dimensional numerical model of the tropical cyclone

    Anthes, R. A., 1972: Development of asymmetries in a three-dimensional numerical model of the tropical cyclone. Monthly Weather Review, 100 (6), 461--476

    work page 1972

  5. [5]

    A., and D

    Anthes, R. A., and D. R. Johnson, 1968: Generation of available potential energy in H urricane H ilda. Monthly Weather Review, 96 (5)

    work page 1968

  6. [6]

    Bhalachandran, S., Z. S. Haddad, S. M. Hristova-Veleva, and F. D. Marks Jr., 2018: The relative importance of factors influencing tropical cyclone rapid intensity changes. Geophysical Research Letters, 46, doi:10.1029/2018GL079997, https://agupubs.onlinelibrary.wiley.com/doi/pdf/10.1029/2018GL079997

    work page doi:10.1029/2018gl079997 2018

  7. [7]

    Nadimpalli, K

    Bhalachandran, S., R. Nadimpalli, K. K. Osuri, F. Marks Jr, S. G. Gopalakrishnan, S. Subramanian, U. C. Mohanty, and D. Niyogi, 2019 a : On the processes influencing rapid intensity changes of tropical cyclones over the B ay of B engal. Scientific Reports, 9 (3382), doi:10.1038/s41598-019-40332-z

    work page doi:10.1038/s41598-019-40332-z 2019

  8. [8]

    Rao, and F

    Bhalachandran, S., P. Rao, and F. Marks Jr, 2019 b : A conceptual framework for the scale-specific stochastic modeling of transitions in tropical cyclone intensities. Earth and Space Science, 6 (6), 972--981

    work page 2019

Show all 81 references
  1. [9]

    HWRF Development Testbed Center Tech

    Biswas, M., and Coauthors, 2016: Hurricane weather research and forecasting (hwrf) model: 2016 scientific documentation. HWRF Development Testbed Center Tech. Rep, https://dtcenter.org/HurrWRF/users/docs/scientific_documents/

    2016

  2. [10]

    A., 2002: A cloud-resolving simulation of hurricane bob (1991): Storm structure and eyewall buoyancy

    Braun, S. A., 2002: A cloud-resolving simulation of hurricane bob (1991): Storm structure and eyewall buoyancy. Monthly Weather Review, 130 (6), 1573--1592

    1991

  3. [11]

    Byrne, D., and J. A. Zhang, 2013: Height-dependent transition from 3- D to 2- D turbulence in the hurricane boundary layer. Geophysical Research Letters, 40 (7), 1439--1442

    2013

  4. [12]

    Chavas, D. R., N. Lin, and K. Emanuel, 2015: A model for the complete radial structure of the tropical cyclone wind field. P art I : Comparison with observed structure. Journal of the Atmospheric Sciences, 72 (9), 3647--3662

    2015

  5. [13]

    Chen, S. S., J. A. Knaff, and F. D. Marks Jr, 2006: Effects of vertical wind shear and storm motion on tropical cyclone rainfall asymmetries deduced from trmm. Monthly Weather Review, 134 (11), 3190--3208

    2006

  6. [14]

    Yau, 2001: Spiral bands in a simulated hurricane

    Chen, Y., and M. Yau, 2001: Spiral bands in a simulated hurricane. P art I : Vortex rossby wave verification. Journal of the Atmospheric sciences, 58 (15), 2128--2145

    2001

  7. [15]

    Corbosiero, K. L., J. Molinari, A. R. Aiyyer, and M. L. Black, 2006: The structure and evolution of hurricane elena (1985). P art II : Convective asymmetries and evidence for vortex rossby waves. Monthly weather Review, 134 (11), 3073--3091

    1985

  8. [16]

    C., and R

    Didlake, A. C., and R. A. Houze, 2013: Convective-scale variations in the inner-core rainbands of a tropical cyclone. Journal of the Atmospheric Sciences, 70 (2), 504--523

    2013

  9. [17]

    Dubey, S., T. N. Krishnamurti, and V. Kumar, 2018: On scale interactions between the MJO and synoptic scale. Quarterly Journal of the Royal Meteorological Society, 144 (717), 2727--2747

    2018

  10. [18]

    A., 1986: An air-sea interaction theory for tropical cyclones

    Emanuel, K. A., 1986: An air-sea interaction theory for tropical cyclones. P art I : Steady-state maintenance. Journal of the Atmospheric Sciences, 43 (6), 585--605

    1986

  11. [19]

    A., 1991: The theory of hurricanes

    Emanuel, K. A., 1991: The theory of hurricanes. Annual Review of Fluid Mechanics, 23 (1), 179--196

    1991

  12. [20]

    M., and S

    Finocchio, P. M., and S. J. Majumdar, 2017: The predictability of idealized tropical cyclones in environments with time-varying vertical wind shear. Journal of Advances in Modeling Earth Systems, 9 (8), 2836--2862

    2017

  13. [21]

    M., and E

    Frank, W. M., and E. A. Ritchie, 2001: Effects of vertical wind shear on the intensity and structure of numerically simulated hurricanes. Monthly Weather Review, 129 (9), 2249--2269

    2001

  14. [22]

    K., 2013: Lectures in turbulence for the 21st century

    George, W. K., 2013: Lectures in turbulence for the 21st century. Chalmers University of Technology

    2013

  15. [23]

    Gopalakrishnan, S. G., F. Marks Jr, X. Zhang, J.-W. Bao, K.-S. Yeh, and R. Atlas, 2011: The experimental HWRF system: A study on the influence of horizontal resolution on the structure and intensity changes in tropical cyclones using an idealized framework. Monthly Weather Rev...

    2011

  16. [24]

    Guimond, S. R., G. M. Heymsfield, and F. J. Turk, 2010: Multiscale observations of hurricane D ennis (2005): The effects of hot towers on rapid intensification. Journal of the Atmospheric Sciences, 67 (3), 633--654

    2005

  17. [25]

    McIntyre, 1987: On the evolution of vorticity and potential vorticity in the presence of diabatic heating and frictional or other forces

    Haynes, P., and M. McIntyre, 1987: On the evolution of vorticity and potential vorticity in the presence of diabatic heating and frictional or other forces. Journal of the Atmospheric Sciences, 44 (5), 828--841

    1987

  18. [26]

    Schubert, S

    Hendricks, E., W. Schubert, S. Fulton, and B. McNoldy, 2010: Spontaneous-adjustment emission of inertia-gravity waves by unsteady vortical motion in the hurricane core. Quarterly Journal of the Royal Meteorological Society, 136 (647), 537--548

    2010

  19. [27]

    vortical

    Hendricks, E. A., M. T. Montgomery, and C. A. Davis, 2004: The role of “vortical” hot towers in the formation of tropical cyclone D iana (1984). Journal of the Atmospheric Sciences, 61 (11), 1209--1232

    1984

  20. [28]

    A., W.-C

    Houze, R. A., W.-C. Lee, and M. M. Bell, 2009: Convective contribution to the genesis of hurricane O phelia (2005). Monthly Weather Review, 137 (9), 2778--2800

    2005

  21. [29]

    C., 1995: The evolution of vortices in vertical shear

    Jones, S. C., 1995: The evolution of vortices in vertical shear. I : Initially barotropic vortices. Quarterly Journal of the Royal Meteorological Society, 121 (524), 821--851

    1995

  22. [30]

    Judt, F., and S. S. Chen, 2016: Predictability and dynamics of tropical cyclone rapid intensification deduced from high-resolution stochastic ensembles. Monthly Weather Review, 144 (11), 4395--4420

    2016

  23. [31]

    Judt, F., S. S. Chen, and J. Berner, 2016: Predictability of tropical cyclone intensity: scale-dependent forecast error growth in high-resolution stochastic kinetic-energy backscatter ensembles. Quarterly Journal of the Royal Meteorological Society, 142 (694), 43--57

    2016

  24. [32]

    DeMaria, 2003: Large-scale characteristics of rapidly intensifying tropical cyclones in the N orth A tlantic basin

    Kaplan, J., and M. DeMaria, 2003: Large-scale characteristics of rapidly intensifying tropical cyclones in the N orth A tlantic basin. Weather and forecasting, 18 (6), 1093--1108

    2003

  25. [33]

    N., 1941: On the degeneration of isotropic turbulence in an incompressible viscous fluid

    Kolmogorov, A. N., 1941: On the degeneration of isotropic turbulence in an incompressible viscous fluid. Dokl. Akad. Nauk SSSR, Vol. 31, 319--323

    1941

  26. [34]

    P., and W

    Kossin, J. P., and W. H. Schubert, 2001: Mesovortices, polygonal flow patterns, and rapid pressure falls in hurricane-like vortices. Journal of the Atmospheric Sciences, 58 (15), 2196--2209

    2001

  27. [35]

    Kossin, J. P., W. H. Schubert, and M. T. Montgomery, 2000: Unstable interactions between a hurricane’s primary eyewall and a secondary ring of enhanced vorticity. Journal of the Atmospheric Sciences, 57 (24), 3893--3917

    2000

  28. [36]

    Roy Bhowmik, 2013: Large-scale characteristics of rapidly intensifying tropical cyclones over the B ay of B engal and a rapid intensification (RI) index

    Kotal, S., and S. Roy Bhowmik, 2013: Large-scale characteristics of rapidly intensifying tropical cyclones over the B ay of B engal and a rapid intensification (RI) index. Mausam, 64 (1), 13--24

    2013

  29. [37]

    Pattnaik, L

    Krishnamurti, T., S. Pattnaik, L. Stefanova, T. V. Kumar, B. P. Mackey, A. O’shay, and R. J. Pasch, 2005: The hurricane intensity issue. Monthly Weather Review, 133 (7), 1886--1912

    2005

  30. [38]

    Simon, M

    Krishnamurti, T., A. Simon, M. Kanti Biswas, and C. Davis, 2012: Impacts of cloud flare-ups on hurricane intensity resulting from departures from balance laws. Tellus A: Dynamic Meteorology and Oceanography, 64 (1), 18\,399

    2012

  31. [39]

    C., and W

    Kwon, Y. C., and W. M. Frank, 2005: Dynamic instabilities of simulated hurricane-like vortices and their impacts on the core structure of hurricanes. part i: Dry experiments. Journal of the atmospheric sciences, 62 (11), 3955--3973

    2005

  32. [40]

    Gopalakrishnan, J

    Leighton, H., S. Gopalakrishnan, J. A. Zhang, R. F. Rogers, Z. Zhang, and V. Tallapragada, 2018: Azimuthal distribution of deep convection, environmental factors, and tropical cyclone rapid intensification: A perspective from HWRF ensemble forecasts of hurricane edouard (2014)...

    2014

  33. [41]

    N., 1955: Available potential energy and the maintenance of the general circulation

    Lorenz, E. N., 1955: Available potential energy and the maintenance of the general circulation. Tellus, 7 (2), 157--167

    1955

  34. [42]

    Marks, F. D., P. G. Black, M. T. Montgomery, and R. W. Burpee, 2008: Structure of the eye and eyewall of hurricane hugo (1989). Monthly Weather Review, 136 (4), 1237--1259

    1989

  35. [43]

    D., and R

    Marks, F. D., and R. A. Houze, 1984: Airborne doppler radar observations in hurricane debby. Bulletin of the American Meteorological Society, 65 (6), 569--582

    1984

  36. [44]

    Marks, F. D., R. A. Houze Jr, and J. F. Gamache, 1992: Dual-aircraft investigation of the inner core of H urricane N orbert. P art I : Kinematic structure. Journal of the Atmospheric sciences, 49 (11), 919--942

    1992

  37. [45]

    Takemi, 2015: A triggering mechanism for rapid intensification of tropical cyclones

    Miyamoto, Y., and T. Takemi, 2015: A triggering mechanism for rapid intensification of tropical cyclones. Journal of the Atmospheric Sciences, 72 (7), 2666--2681

    2015

  38. [46]

    D., and M

    M \"o ller, J. D., and M. T. Montgomery, 1999: Vortex rossby waves and hurricane intensification in a barotropic model. Journal of the Atmospheric Sciences, 56 (11), 1674--1687

    1999

  39. [47]

    Nicholls, T

    Montgomery, M., M. Nicholls, T. Cram, and A. Saunders, 2006: A vortical hot tower route to tropical cyclogenesis. Journal of the Atmospheric sciences, 63 (1), 355--386

    2006

  40. [48]

    T., and R

    Montgomery, M. T., and R. J. Kallenbach, 1997: A theory for vortex rossby-waves and its application to spiral bands and intensity changes in hurricanes. Quarterly Journal of the Royal Meteorological Society, 123 (538), 435--465

    1997

  41. [49]

    T., and R

    Montgomery, M. T., and R. K. Smith, 2017: Recent developments in the fluid dynamics of tropical cyclones. Annual Review of Fluid Mechanics, 49, 541--574

    2017

  42. [50]

    Moon, Y., and D. S. Nolan, 2010: Do gravity waves transport angular momentum away from tropical cyclones? Journal of the Atmospheric Sciences, 67 (1), 117--135

    2010

  43. [51]

    Munsell, E. B., F. Zhang, J. A. Sippel, S. A. Braun, and Y. Weng, 2017: Dynamics and predictability of the intensification of hurricane edouard (2014). Journal of the Atmospheric Sciences, 74 (2), 573--595

    2014

  44. [52]

    S., and L

    Nolan, D. S., and L. D. Grasso, 2003: Nonhydrostatic, three-dimensional perturbations to balanced, hurricane-like vortices. P art II : Symmetric response and nonlinear simulations. Journal of the Atmospheric sciences, 60 (22), 2717--2745

    2003

  45. [53]

    Nolan, D. S., Y. Moon, and D. P. Stern, 2007: Tropical cyclone intensification from asymmetric convection: Energetics and efficiency. Journal of the Atmospheric Sciences, 64 (10), 3377--3405

    2007

  46. [54]

    V., 1982: Conceptual evolution of the theory and modeling of the tropical cyclone

    Ooyama, K. V., 1982: Conceptual evolution of the theory and modeling of the tropical cyclone. Journal of the Meteorological Society of Japan. Ser. II, 60 (1), 369--380

    1982

  47. [55]

    Osuri, K. K., R. Nadimpalli, U. C. Mohanty, and D. Niyogi, 2017: Prediction of rapid intensification of tropical cyclone phailin over the bay of bengal using the hwrf modeling system. Quarterly Journal of the Royal Meteorological Society, 143 (703), 678--690

    2017

  48. [56]

    Persing, J., M. T. Montgomery, J. McWilliams, and R. K. Smith, 2013: Asymmetric and axisymmetric dynamics of tropical cyclones. Atmos. Chem. Phys, 13 (12), 299--12

    2013

  49. [57]

    Malkus, 1961: Some aspects of hurricane D aisy, 1958

    Riehl, H., and J. Malkus, 1961: Some aspects of hurricane D aisy, 1958. Tellus, 13 (2), 181--213

    1961

  50. [58]

    Riemer, M., and M. T. Montgomery, 2011: Simple kinematic models for the environmental interaction of tropical cyclones in vertical wind shear. Atmospheric Chemistry and Physics, 11 (17), 9395

    2011

  51. [59]

    Riemer, M., M. T. Montgomery, and M. E. Nicholls, 2010: A new paradigm for intensity modification of tropical cyclones: thermodynamic impact of vertical wind shear on the inflow layer. Atmospheric Chemistry & Physics, 10 (7)

    2010

  52. [60]

    Ryglicki, D. R., J. Cossuth, D. Hodyss, and J. D. Doyle, 2018 a : The unexpected rapid intensification of tropical cyclones in moderate vertical wind shear. part i: Overview and observations. Monthly Weather Review, 146 (11), 3773--3800

    2018

  53. [61]

    Ryglicki, D. R., J. D. Doyle, Y. Jin, D. Hodyss, and J. Cossuth, 2018 b : The unexpected rapid intensification of tropical cyclones in moderate vertical wind shear. P art II : Vortex tilt. Monthly Weather Review, 146 (11), 3801--3825

    2018

  54. [62]

    R., and D

    Ryglicki, D. R., and D. Hodyss, 2016: A deeper analysis of center-finding techniques for tropical cyclones in mesoscale models. part i: Low-wavenumber analysis. Journal of Applied Meteorology and Climatology, 55 (3), 531--559

    2016

  55. [63]

    Journal of Meteorology, 14 (6), 513--523

    Saltzman, B., 1957: Equations governing the energetics of the larger scales of atmospheric turbulence in the domain of wave number. Journal of Meteorology, 14 (6), 513--523

    1957

  56. [64]

    Schubert, W. H., M. T. Montgomery, R. K. Taft, T. A. Guinn, S. R. Fulton, J. P. Kossin, and J. P. Edwards, 1999: Polygonal eyewalls, asymmetric eye contraction, and potential vorticity mixing in hurricanes. Journal of the atmospheric sciences, 56 (9), 1197--1223

    1999

  57. [65]

    B., and M

    Smith, G. B., and M. T. Montgomery, 1995: Vortex axisymmetrization: Dependence on azimuthal wave-number or asymmetric radial structure changes. Quarterly Journal of the Royal Meteorological Society, 121 (527), 1615--1650

    1995

  58. [66]

    K., and M

    Smith, R. K., and M. T. Montgomery, 2010: Hurricane boundary-layer theory. Quarterly Journal of the Royal Meteorological Society, 136 (652), 1665--1670

    2010

  59. [67]

    K., and M

    Smith, R. K., and M. T. Montgomery, 2016: The efficiency of diabatic heating and tropical cyclone intensification. Quarterly Journal of the Royal Meteorological Society, 142 (698), 2081--2086

    2016

  60. [68]

    Smith, R. K., J. A. Zhang, and M. T. Montgomery, 2017: The dynamics of intensification in a hurricane weather research and forecasting simulation of hurricane E arl (2010). Quarterly Journal of the Royal Meteorological Society, 143 (702), 293--308

    2010

  61. [69]

    P., and N

    Starr, V. P., and N. E. Gaut, 1970: Negative viscosity. Scientific American, 223 (1), 72--83

    1970

  62. [70]

    B., 2012: An introduction to boundary layer meteorology, Vol

    Stull, R. B., 2012: An introduction to boundary layer meteorology, Vol. 13. Springer Science & Business Media

    2012

  63. [71]

    Emanuel, 2010: Midlevel ventilation’s constraint on tropical cyclone intensity

    Tang, B., and K. Emanuel, 2010: Midlevel ventilation’s constraint on tropical cyclone intensity. Journal of the Atmospheric Sciences, 67 (6), 1817--1830

    2010

  64. [72]

    Emanuel, 2012: Sensitivity of tropical cyclone intensity to ventilation in an axisymmetric model

    Tang, B., and K. Emanuel, 2012: Sensitivity of tropical cyclone intensity to ventilation in an axisymmetric model. Journal of the Atmospheric Sciences, 69 (8), 2394--2413

    2012

  65. [73]

    Van Sang, N., R. K. Smith, and M. T. Montgomery, 2008: Tropical-cyclone intensification and predictability in three dimensions. Quarterly Journal of the Royal Meteorological Society, 134 (632), 563--582

    2008

  66. [74]

    T., and G

    Vonich, P. T., and G. J. Hakim, 2018: Hurricane kinetic energy spectra from in situ aircraft observations. Journal of the Atmospheric Sciences, 75 (8), 2523--2532

    2018

  67. [75]

    Journal of the Atmospheric Sciences, 34 (7), 1028--1039

    Willoughby, H., 1977: Inertia-buoyancy waves in hurricanes. Journal of the Atmospheric Sciences, 34 (7), 1028--1039

    1977

  68. [76]

    Willoughby, H. E., F. D. Marks Jr, and R. J. Feinberg, 1984: Stationary and moving convective bands in hurricanes. Journal of the Atmospheric sciences, 41 (22), 3189--3211

    1984

  69. [77]

    M., and E

    Wood, K. M., and E. A. Ritchie, 2015: A definition for rapid weakening of N orth A tlantic and eastern N orth P acific tropical cyclones. Geophysical Research Letters, 42 (22), 10--091

    2015

  70. [78]

    Liu, and Y

    Wu, L., Q. Liu, and Y. Li, 2018: Prevalence of tornado-scale vortices in the tropical cyclone eyewall. Proceedings of the National Academy of Sciences, 115 (33), 8307--8310

    2018

  71. [79]

    Kosiba, 2018: The role of small-scale vortices in enhancing surface winds and damage in H urricane H arvey (2017)

    Wurman, J., and K. Kosiba, 2018: The role of small-scale vortices in enhancing surface winds and damage in H urricane H arvey (2017). Monthly Weather Review, 146 (3), 713--722

    2017

  72. [80]

    Wang, and B

    Yang, B., Y. Wang, and B. Wang, 2007: The effect of internally generated inner-core asymmetries on tropical cyclone potential intensity. Journal of the Atmospheric Sciences, 64 (4), 1165--1188

    2007

  73. [81]

    Tao, 2013: Effects of vertical wind shear on the predictability of tropical cyclones

    Zhang, F., and D. Tao, 2013: Effects of vertical wind shear on the predictability of tropical cyclones. Journal of the Atmospheric Sciences, 70 (3), 975--983

    2013

Pith tools

Reviewed August 14, 2026 · model on record in the stance chip above.