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Convection Initiation (Some Theory & Fundamentals). Stan Trier NCAR (MMM Division). Outline. Assessment of vertical stability a. Review of parcel theory and conditional instability i. CAPE, CIN and Skew-T (sounding) diagrams b. Potential instability and layer lifting

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Convection Initiation (Some Theory & Fundamentals)

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Convection initiation some theory fundamentals

Convection Initiation (Some Theory & Fundamentals)

Stan Trier

NCAR (MMM Division)


Outline

Outline

  • Assessment of vertical stability

    a. Review of parcel theory and conditional instability

    i. CAPE, CIN and Skew-T (sounding) diagrams

    b. Potential instability and layer lifting

  • Thermodynamic destabilization processes

    a. Equations for moisture and lapse rate change

    b. Physical processes

    i. Turbulent heat and moisture fluxes

    ii. Horizontal advections

    iii. Vertical motions

    3.Broad categories of vertical motion mechanisms


Parcel theory assumptions

Parcel Theory (Assumptions)

  • Vertically displaced air exchanges no mass or heat with surroundings

  • Instantaneous adjustment to the ambient pressure

  • Subsaturated air parcels change temperature at dry adiabatic lapse rate

  • Saturated air parcels change temperature at moist adiabatic lapse rate

    which ranges from ~ 4 K / km (warm lower troposphere) to ~ 10 K / km

  • Vertical accelerations governed only by the buoyancy force


Parcel theory cont definitions

Parcel Theory Cont. (Definitions)

  • Conditional Instability:

    Vertical displacement must be sufficient to saturate the air parcel, whereby the reduced rate of cooling upon subsequent ascent would allow the parcel to eventually become positively buoyant

  • Lifting Condensation Level (LCL): An air parcel (which conserves ) becomes saturated at this level (owing to adiabatic cooling) if given a sufficient upward displacement

  • Level of Free Convection (LFC): Level at which vertically displaced air parcel becomes warmer than ambient atmosphere and subsequently accelerates vertically due to positive buoyancy

  • Level of Neutral Buoyancy (LNB): Level at which ascending air parcel becomes colder than ambient atmosphere and decelerates vertically due to negative buoyancy


Parcel theory cont definitions1

Parcel Theory Cont. (Definitions)

Parcel theory assumes complete conversion of potential to kinetic energy

Strength of vertical motion required to raise air parcel to its LFC


Example skew t diagrams

Example Skew-T Diagrams

Central U.S. Warm-Season

Oceanic Tropical

  • Characteristics (CAPE=2750 J/kg, CIN=110 J/Kg):

  • Moderate PBL RH

  • Stable layer above PBL

  • Steep midtropospheric lapse rate (very unstable)

  • Characteristics (CAPE=1000 J/kg, CIN=10 J/Kg):

  • High PBL RH

  • No stable layer above PBL

  • Nearly moist-neutral lapse rate (slightly unstable)

LIttle lifting required

Deep lifting required


Some other examples

Some Other Examples

Western U.S. Warm Season

Central U.S. “Elevated” Instability

  • Deep, dry PBL with moist midlevels

  • Strong downdraft, wind potential, little rain

  • Most unstable air with little CIN located above PBL

  • Common at night and north of warm/stationary fronts


Convection initiation some theory fundamentals

Boundary Layer Temperature / Moisture Effects on CAPE and Vertical Velocity

Parcel theory predicts complete conversion of

buoyancy to kinetic energy with wmax = (2 CAPE)1/2

  • Positive buoyancies occur under saturated conditions

Moist static energy (h = gz + cpT+ Lq) conserved

Since L / cp ~ 2.5

r = 0.9

Rough equivalence of boundary layer Temp

and moisture effects on storm strength

in well-developed convection cases

From Crook (1996), Mon. Wea. Rev.


Convection initiation some theory fundamentals

Boundary Layer Temperature / Moisture Effects on Convection Inhibition (CIN)

When LCL is above boundary layer, CIN does not depend uniquelyon moist static energy


Convection initiation some theory fundamentals

More Boundary Layer Temperature / Moisture Effects on Convection Inhibition (CIN)

Quantification from Crook (1996):

For temperature and moisture increases of equal moist static energy

Some limiting cases:


Some limitations of parcel theory

Some Limitations of Parcel Theory

  • Tends to overestimate convective strength (vertical velocities) or triggering

    - no consideration of dry entrainment, water loading, adverse VPGFs

  • Cases with limited CAPE can produce very strong convection

    - strong forcing features (e.g., sharp fronts) and strong environmental

    vertical shear can produce favorable VPGFs

  • Most applicable to conditionally unstable air parcels in localized regions

    - convection may also occur in rapidly evolving environments with potential

    instability when deep layer lifting occurs


Case of a severe frontal rainband with negligible cape

Case of a Severe Frontal Rainband with Negligible CAPE

From Carbone (1982, J. Atmos. Sci.)


Some limitations of parcel theory1

Some Limitations of Parcel Theory

  • Tends to overestimate convective strength (vertical velocities) or triggering

    - no consideration of dry entrainment, water loading, adverse VPGFs

  • Cases with limited CAPE can produce very strong convection

    - strong forcing features (e.g., sharp fronts) and strong environmental

    vertical shear can produce favorable VPGFs

  • Most applicable to conditionally unstable air parcels in localized regions

    - convection may also occur in rapidly evolving environments with potential

    instability when deep layer lifting occurs


Convection initiation some theory fundamentals

Effects of Layer Lifting on Potentially Unstable Sounding

  • Initial Sounding:

  • No CAPE for any parcels

  • Final Sounding:

  • Deep Moist Absolutely

  • Unstable Layer (MAUL)

  • Positive CAPE w/ no CIN

Layer Lifting

From Bryan and Fritsch (2000, BAMS)


Thermodynamic destabilization

Thermodynamic Destabilization

  • Forecasting of CI is hampered by limited availability of sounding information in space and time

  • Knowledge of physical processes must generally be used to anticipate local evolution of thermodynamic stability

  • Both CAPE and CIN are sensitive to the lapse rate and the lower-tropospheric moisture


Moisture tendency equation

Moisture Tendency Equation

mean advection

eddy flux

convergence

diabatic

sources


Lapse rate tendency equation

Lapse Rate Tendency Equation

differential

horizontal

advection

differential

vertical

motion

differential

diabatic

forcing


Turbulent heat and moisture fluxes

Turbulent Heat and Moisture Fluxes

  • PBL growth depends on several

  • factors including:

  • vigor of turbulent eddies

  • stability of air above PBL

Daytime heating results in increase

of PBL depth and potential temperature


Turbulent heat and moisture fluxes cont

Turbulent Heat and Moisture Fluxes (Cont.)

  • In quiescent conditions the vertical moisture flux convergence < 0

  • term can be critical

  • Unlike q, qv decreases above PBL

  • When not balanced by surface

  • evaporation or moisture advection,

  • as PBL grows qv can decrease

  • significantly due to vertical flux term

  • Large temporal decreases most

  • common when dry air exists above

  • PBL and inversion is not too strong

In this example vertical heat flux convergence > 0 in PBL helps eliminate

CIN but the strong drying from vertical moisture flux reduces PBL CAPE


Turbulent heat and moisture fluxes cont1

Turbulent Heat and Moisture Fluxes (Cont.)

  • Different Example (Day Before, Same Location and Quiescent Synoptic Condition)

  • Stronger initial inversion and moister

  • conditions above the PBL than

  • previous example

  • No temporal drop in PBL qv

In this example, the heating/vertical mixing process also reduces CIN but this time

results in increased PBL CAPE


Heating gradients and induced circulations

Heating Gradients and Induced Circulations

Numerical Simulation

Cloud Streets

  • Simulation indicates convective initiation

  • within 100-200 km zone of PBL rolls

  • near surface moisture gradient (dryline)

Deep

Convective

Initiation

From Trier, Chen and Manning (2004, Mon. Wea. Rev.)


Heating gradients and induced circulations1

Heating Gradients and Induced Circulations

1000-1400 CST Time-Averaged Sfc Heat Flux

Legend: Color Shading (updrafts 2 cm/s intervals)

Green Lines (downdrafts 2 cm/s intervals)

Labeled Black Lines (Winds in cross-section)

From Trier, Chen and Manning (2004, Mon. Wea. Rev.)


Heating gradients and induced circulations2

Heating Gradients and Induced Circulations

Legend: Color Shading (updrafts 2 cm/s intervals)

Green Lines (downdrafts 2 cm/s intervals)

Labeled Black Lines (Winds in cross-section)

From Trier, Chen, and Manning (2004, Mon. Wea. Rev.)


Terrain influence on timing of convection initiation

Terrain Influence on Timing of Convection Initiation

  • Daytime convection over “lowlands” typically

  • begins later than over adjacent terrain due

  • to greater surface heating required

  • Mountain high-level heat source may help

  • initiate solenoidal circulation in which ascent

  • and moisture transport occur over slope

  • Convection over “lowlands” more intense due

  • to greater CAPE

Mtn. Top

Plains

AC – Dry adiabat from sfc convective temperature to CCL

EG – Dry adiabat from mtn convective temperature to CCL

Hatched Areas – Energy Input required to reach convective

temperature at different elevations

From Bluestein (1993) Synoptic-Dynamic Meteorology in Midlatitudes Vol. II


Influence of vertical motions

Influence of Vertical Motions

22 LST Surface q / Winds / Reflectivity

  • Afternoon sounding conditionally unstable

  • but with stable layer above PBL

  • Lifting above frontal surface contributes to

  • 100-deep unstable “saturated” layer that

  • allows development of E-W oriented

  • nocturnal convective band

  • Here, the lifting both 1) transports moisture

  • in the vertical, raising the RH as ascending

  • air adiabatically cools, and 2) steepens the

  • midtropospheric lapse rate, which together

  • allow organized convection to proceed

Sounding location


Lifting and horizontal advection of moisture

Lifting and Horizontal Advection of Moisture

02 LST Surface q / Winds/ Reflectivity

  • Another case of nocturnal convection along

  • and north of a quasi-stationary surface front

  • Unlike previous case, lifting alone cannot

  • explain local evolution of the sounding

  • Here, the MAUL has mixing ratio values much

  • greater than at any level in the 6-h old sounding

  • indicating importance of horizontal advection

Sounding location


Convection initiation some theory fundamentals

  • Environmental lower-tropospheric ascent (at some horizontal scale) generally required to initiate organized convection

  • In many cases mesoscale vertical motion is important in allowing organized convection to persist beyond several cycles of convective cells (caveat, self-sustaining convection in strong shear)


Forced isentropic mesoscale ascent

Forced (Isentropic) Mesoscale Ascent

  • Occurs with horizontal warm temperature advection

    - Can saturate conditionally or potentially unstable lower-tropospheric layers (direct initiation)

    - Can reduce CIN defining where fine-scale mechanisms can more easily initiate convection (indirect initiation)

    - May be orographically forced or associated with overrunning of statically stable air masses

  • Examples:

    - Relative flow up frontal surfaces (e.g., Low-level jets)

    - Mesoscale convective vortices (MCVs)


Convection initiation some theory fundamentals

Raymond and Jiang (JAS 1990) Conceptual Model of Isentropic

Lifting within a Steady Balanced Vortex (e.g., MCV)


Solenoidal circulations

Solenoidal Circulations

  • Thermally-direct atmospheric flows forced by baroclinity

    - under hydrostatic conditions strength is governed by horizontal temperature gradient and depth through which it extends

    - often associated with differential surface heating

  • Sources:

    - sloped or irregular terrain (e.g., mountain-valley circulation)

    - land-water contrasts (e.g., sea-breezes)

    - land-surface contrasts (e.g., vegetative differences, soil moisture gradients)

    - spatial variations in cloudiness

    - antecedent convection (e.g., gust fronts)


Sea breeze circulation

Sea-Breeze Circulation


Gravity waves and related phenomena

Gravity Waves and Related Phenomena

  • Unbalanced circulations resulting from convection and

    other sources

  • Examples related to convective sources

    - Deep (full tropospheric)

    - Shallow (trapped)


Deep full tropospheric gravity waves

Deep (Full-Tropospheric) Gravity Waves

Vertical Motion Associated with MCS-like Vertical Heating Profile

Lower-tropospheric ascent

near MCS

Deep subsidence

farther away

L

  • L=1 mode associated with convective part of heating profile has rapid phase speed

  • L=2 mode associated with stratiform component of MCS heating profile has slower

  • phase speed (~ 20 m/s) and may cause vertical displacements sufficient to destabilize

  • initially small CIN environments

From Mapes (1993) J. Atmos. Sci.


Shallow trapped wave like disturbances

Shallow (Trapped) Wave-Like Disturbances

Internal Bore of

Wavelength

Density Current

  • Gravity-wave related phenomena can be excited by antecedent convection

  • Statically stable nocturnal PBL provides an environment where such

  • disturbances can maintain coherence

From Simpson (1997), An Introduction to Atmospheric Density Currents


Turbulent pbl based circulations

Turbulent PBL-Based Circulations

  • In situations with little or no CIN, PBL-based circulations can determine where deep convection first initiates

  • Horizontal convective roll circulations (for example) have differences in potential temperature and moisture between ascending and subsiding branches

  • Can define sites where deep convective clouds form on mesoscale boundaries


Hcrs intersecting sea breeze front

HCRs Intersecting Sea-Breeze Front

From Atkins et al. (1995) Mon. Wea. Rev.


Thank you

Thank You!

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