dr. charles a. doswell iii ou/cimms/doswell scientific consulting … · 2017. 1. 5. · dr....
TRANSCRIPT
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Dr. Charles A. Doswell III OU/CIMMS/Doswell Scientific Consulting - Norman, Oklahoma USA
European Conf. on Severe Storms – 07 October 2011
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A fundamental assump.on
• In the physical world (not at the quantum scale!), nothing happens – Randomly – For no physical purpose
• Atmospheric processes – examples – Extratropical cyclones – Deep, moist convec.ve storms – Tropical cyclones – Gravity waves – … etc. …
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ETCs - always present
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What are ETCs for?
• Baroclinic instability (Charney/Eady theory) – Available poten.al energy (APE) – Meridional temperature gradient / ver.cal shear – Sta.c stability is a factor
• Kine.c energy of disturbance drawn from APE – “Self-‐development” early in the life cycle – Redistributes solar heat input so as to reduce the meridional temperature gradient
– Ver.cal mo.on leads to increasing sta.c stability
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Neutral Stability Curve
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Varying Sta.c Stability
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Deep, moist convec.on (DMC)
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What is DMC for?
• Buoyant instability – Parcel theory – Convec.ve available poten.al energy (CAPE) – Ver.cal gradients of temperature and moisture
• Kine.c energy of disturbance drawn from CAPE – Redistributes heat and moisture ver.cally
• IntermiWent – only when needed (ingredients)
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Tropical Cyclones
• Basically, a heat engine
• Involves DMC
• Transfers heat from the oceans into the atmosphere
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Supercells – why?
• Obviously, also associated with CAPE and buoyant instability
• Defini.on of a supercell: – Deep, persistent mesocyclone
• Significant frac.on of ver.cal depth of DMC
• Persists > convec.ve .me scale, τc • Vor.city ~ 1 x 10-‐2 s-‐1
• A helical flow – begins as a rota.ng updraa
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A supercell
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Supercell characteris.cs
• Only about 20-‐25% of supercells are tornadic • Most DMC storms are not supercells
– Supercell rota.on is a result of pre-‐exis.ng (environmental) horizontal vor.city being .lted into the ver.cal by ver.cal draas -‐ updraa becomes helical
• Supercells have a significant contribu.on to their ver.cal mo.on from a non-‐buoyant source: updraa/ver.cal shear interac.ons
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Buoyancy and perturba.on pressure • Parcel theory:
€
dwdt B
= g Tv − T vT v
≡ B
€
dwdt
= −1ρ∂ ʹ′ p b∂z
+∂ ʹ′ p d∂z
⎡
⎣ ⎢ ⎤
⎦ ⎥ + B
= −1ρ∂ ʹ′ p d∂z
i
+−1ρ∂ ʹ′ p b∂z
+ B⎡
⎣ ⎢
⎤
⎦ ⎥
ii
,
Doswell and Markowski (2004)
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What do supercells do?
• Mi.ga.ng CAPE is not the only answer – Mul.ple passages of tornadic supercells over nearly the same track
– “Clearing” squall lines oaen signal the end of storm ac.vity
– If that’s all that supercells are doing, it would fail to explain what supercells do that ordinary DMC does not do
– The key is helicity and the fact that a supercell is dominated by a rota.ng, helical updraa
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Classic supercells and buoyancy
10 Feb 2009 KTLC radar
1
2
3
4
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What are supercells for?
• Some energy of the supercell is drawn from a reservoir of CAPE
• Helicity, H, can be interpreted as a form of poten2al energy – owing to the distribu.on of airflow – units of energy per unit mass (J kg-‐1 or m2 s-‐2) – integrand is streamwise vor2city
€
H z( ) = − Vh −C( ) • k × ∂Vh
∂z⎡
⎣ ⎢ ⎤
⎦ ⎥ z0
z
∫ dz
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• “Stretching” term in the vor.city (ζ) equa.on, when divergence (δ < 0) – i.e., conserva.on of angular momentum
• Exponen.al growth = classical indicator of an instability
Helical flows can be unstable
€
dζdt
= −δζ ⇒ ζ t( ) = ζ0 exp −δt( )
€
∂ω∂p
= −δ = −∂u∂x
+∂v∂y
⎛
⎝ ⎜
⎞
⎠ ⎟
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LND ω
δ
Schema.c supercell ver.cal mo.on (ω)/divergence (δ)
0
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What are supercells for? -‐ cont’d
• Both buoyant instability and “helicity instability” are involved – a synergy – No buoyancy => no DMC – No helicity => nonsupercellular DMC
• All DMC mi.gates buoyant instability • Supercells also mi.gate ‘helicity instability’
– Updraa ingests streamwise vor.city – Vor.city is amplified by stretching (to LND) – Vor.city is deamplified by storm top divergence
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Updraa-‐shear/helicity interac.on
L
Vor.city vectors
Wind vectors
Perturba.on pressure deficit due to increasing vor.city aloa – increased updraa Streamwise vor.city
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Summary for supercells
• Supercells have both buoyant and nonbuoyant poten.al energy available
• Tornadic supercells, in par.cular, can be inefficient at producing pools of stable air at low levels but will “consume” reservoirs of CAPE and helicity
• Supercell consumes helicity by first spinning it up and then spinning it down even more
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Tornado characteris.cs
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Two tornadoes – one supercell
Mesocyclonic tornado
Nonmesocyclonic tornado
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Tornado characeris.cs (cont’d)
• Some tornadoes develop first aloa and develop downward (dynamic pipe)
• Some tornadoes develop first near the surface and develop upward (nonmesocyclonic)
• Some tornadoes form through a deep layer at about the same .me
• Some tornado-‐like vor.ces come close to, but never develop surface-‐based tornadic intensity (“funnel clouds”, TVSs aloa)
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Tornadogenesis research
• Seeks to explain what makes a supercell storm tornadic – Deep layer shear/helicity (e.g., 0-‐6 km) is associated with supercells
– Empirical observa.ons – tornadoes are more likely whenever: • Near-‐surface (e.g., 0-‐1 km) shear/helicity is large • Near-‐surface LCLs are low (r.h. Is high)
• Tornadoes from non-‐supercells
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• CAPE has been proposed – Tornado would be a “parasite” – How much buoyant energy is released by the vortex itself? – .ny compared to updraa
– Some tornadoes have no visible condensa.on funnel below cloud base
– Thermodynamic “speed limit”?
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What do tornadoes do?
• Vor.city is an efficient mixing mechanism on all scales – What is being mixed?
• Not mi.ga.ng CAPE! • ‘Helicity instability’ is likely involved (e.g., short .me scale of tornado development)
– What determines the scale of a tornado? • Is it simply contrac.on and, therefore, amplifica.on of stormscale vor.city?
• Shear instabili.es within mesocyclonic vortex flow?
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Empirical evidence
• The most relevant shear/helicity for discrimina.ng tornadic from non-‐tornadic storms is that very near the surface
• Studies of tornadoes suggest greatest perturba.on pressure drop is above, but very near the surface – upward accelera.ons > 1 g!
• Again sugges.ve of ‘helicity instability’ in the ‘corner flow’ region of the vortex
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Intense radial inflow
Extreme upward accelera.on
Upward vor.city advec.on
L
“spin down” occurs much higher up
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Tornado-‐like vor.ces aloa
• Presumably, some form of ‘helicity instability’ first develops aloa
• Kinema.cs – vortex lines don’t end at the sfc • Condi.ons near the surface don’t permit the vortex to interact strongly with the surface boundary layer – Too nega.vely buoyant – Not enough helicity within the surface boundary layer to intensify the near-‐surface vortex
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Nonmesocyclonic tornadoes
• Pre-‐exis.ng maxima in low-‐level ver.cal vor.city (“misocyclones”)
• Flow becomes helical when an updraa moves over a low-‐level vor.city maximum
• Helicity instability again operates, rapidly crea.ng a deep vortex that begins near the surface
• Low-‐level mesoscale boundaries (fronts, dry lines, gust fronts) can have considerable ver.cal vor.city (ζ ~10-‐3 s-‐1)
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Thank you!! Ques.ons? Contact:
• [email protected] • [email protected]
• hWp://www.flame.org/~cdoswell