A tropical cyclone is the generic term for a hurricane, typhoon, or tropical storm. Tropical cyclones derive their energy from evaporation of water at the ocean surface which ultimately recondenses when it cools to the saturation point. The rotation of a tropical cyclone is caused by the Coriolis effect.

What is unclear to me is: Why do these massive bodies of warm, moist air clump together over thousands of kilometers? What physical process causes them to be drawn in towards the center of the storm?

enter image description here *image taken from the Wikipedia article on tropical cyclones

  • $\begingroup$ The tropical cyclogenesis article on wikipedia describes how cyclones form, but I'm not sure it answers this question. Maybe the answer is just "extreme values of all of the above"? $\endgroup$
    – naught101
    Commented Apr 17, 2014 at 11:00
  • $\begingroup$ angular momentum, is my suspicion. $\endgroup$
    – Neo
    Commented Apr 18, 2014 at 4:25
  • 2
    $\begingroup$ This image shows the evolution of wind pattern in tropical cyclogenesis. The storm eventually becomes large enough for the Coriolis force to balance out the other forces(pressure gradient force), which causes the wind flow to become geostrophic (parallel to isobars) close to the eye of the storm. Tropical systems typically weaken after losing their heat source (ocean), but strong steering flow winds can also shear a hurricane apart by disrupting the aforementioned balance. Illustration of forces $\endgroup$
    – DrewP84
    Commented Apr 18, 2014 at 4:40
  • $\begingroup$ I should clarify that the winds are not truly geostrophic but instead quasi-geostrophic. $\endgroup$
    – DrewP84
    Commented Apr 18, 2014 at 4:50
  • $\begingroup$ @DrewP84 Thanks for the response. Do you want to turn it into a full answer? I'll accept and upvote it if you do. $\endgroup$ Commented Apr 18, 2014 at 16:10

1 Answer 1


The equation of motion for a fluid parcel in the atmosphere (in Cartesian space) is

$$\dfrac{D\mathbf u}{Dt} = -\dfrac{1}{\rho}\nabla p-2 \mathbf \Omega \times \mathbf u + \mathbf g + \mathbf F,$$

where $\mathbf u$ is the wind, $\rho$ is density, $p$ is pressure, $\mathbf\Omega$ is the angular velocity of the Earth, $\mathbf g$ is gravity and $\mathbf F$ is friction. The derivative is a material derivative (Lagrangian perspective) where

$$\dfrac{D\varphi}{Dt} = \dfrac{\partial\varphi}{\partial t} + \mathbf u\cdot\nabla\varphi.$$

There is a non-dimensional number called the Rossby number ($Ro$) that determines when a flow behaves geostrophically. This number is given by

$$Ro = {U\over fL},$$

where $U$ is a velocity scale, $L$ is a length scale and $f$ is the Coriolis parameter ($f=2\Omega\sin\phi$, $\Omega = 7.2921 \times 10^{-5}\ \text{s}^{-1}$, and $\phi$ is latitude). When $Ro << 1$, the flow exhibits geostrophic balance. This occurs when $L$ becomes large, which it does as the storm grows. When I say the flow is geostrophic, what I really mean is that the net acceleration of a parcel is small. In a tropical cyclone the isobars are roughly circular and this curvature gives rise to the gradient wind balance.

The gradient wind is the balance of the pressure gradient force, Coriolis force and centripetal acceleration. In this flow, just as in geostrophic flow, the wind will follow the isobars, flowing cyclonically around the center of low pressure, though slower than a geostrphic flow with the same pressure gradient. Close to the ocean surface friction plays a role, and for the near surface winds the friction will cause the wind to be slightly deflected toward low pressure, or inward across the isobars.

Close to the center of the storm, in and near the eyewall, the length scale $L$ is reduced and the Coriolis force places a smaller role. Here the flow attains cyclostrophic balance -- a balance between centrifugal and pressure gradient forces.

The gradient and cyclostrophic balances explain the wind rotating around the storm and surface friction will give a radially inward component at low levels, advecting angular momentum toward the center of the storm. Convection in the eyewall will lift air to the tropopause where it will flow anti-cyclonically (due to the thermal wind) away from the storm before subsiding. The core of the storm is warm and the air there is subsiding, creating the cloud free eye. The flows around the storm are balanced flows and the flow inward/upward/outward/downward is a thermodynamic carnot engine.

This gives us a fairly stable setup and this is why once a tropical storm forms it tends to persist rather than tear itself apart. The key to sustaining this balance is a warm ocean surface and weak vertical windshear. If you take away the warm ocean the storm will start to spin down and if you have strong shear you will disconnect the lower and upper level circulations and the storm will weaken.

  • 1
    $\begingroup$ +1 This is the correct answer. $\endgroup$ Commented May 4, 2014 at 5:22

Your Answer

By clicking “Post Your Answer”, you agree to our terms of service and acknowledge you have read our privacy policy.

Not the answer you're looking for? Browse other questions tagged or ask your own question.