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Precipitation processes*. Types of precipitation Stratiform Convective – deep (mixed phase) and shallow (warm) Mixed stratiform-convective Organization of precipitation Precipitation theories Mesoscale structure of rain. Nimbostratus and stratiform precipitation.

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Precipitation processes
Precipitation processes*

  • Types of precipitation

    • Stratiform

    • Convective – deep (mixed phase) and shallow (warm)

    • Mixed stratiform-convective

  • Organization of precipitation

  • Precipitation theories

  • Mesoscale structure of rain


Nimbostratus and stratiform precipitation
Nimbostratus and stratiform precipitation

  • Classification of precipitation

    • stratiform: |w| < Vice, where Vice is in the range 1-3 m s-1

      • Vice refers to snow and aggregates

    • convective: |w|  Vice

  • A more detailed classification (see following figure)

    • shallow convection

    • deep convection

    • mixed convective/stratiform

    • (pure) stratiform


Precipitation formation: simple flow chart

Fig. 8.10. Simplified schematic of the precipitation processes active in clouds. Taken from Lamb (2001).

Compare with the complex diagram in thefollowing frame.



A classification scheme based on vertically pointing radar data tokay et al 1999
A classification scheme based on vertically pointing radar data(Tokay et al 1999)

brightband

Z > 10 dBZ

spectrum width


Examples of automated precipitation classification scheme based on the preceding algorithm. From Tokay et al (1999, JAM).


From Tokay et al (1999, JAM). based on the preceding algorithm. From Tokay et al (1999, JAM).


From Tokay et al (1999, JAM). based on the preceding algorithm. From Tokay et al (1999, JAM).


A physical definition of convective vs stratiform precipitation
A physical definition of convective vs. stratiform precipitation

  • Convective precipitation

    • hydrometeors move upwards at some point during the growth phase

    • growth time scale ~20-30 min

    • Rain rate, R > 10 mm hr-1

  • Stratiform precipitation

    • hydrometeors fall during growth

    • R typically 1-5 mm hr-1

    • growth time scale 1-2 h for a deep Ns system

    • significant stratiform precipitation likely requires an ice phase

      • the exception is drizzle from Sc, but this is not significant


The importance of stratiform precipitation
The importance of stratiform precipitation precipitation

  • For the Huntsville region, stratiform precipiation occurs ~99% of the time (large area)

  • A much greater fraction of rain originates from convective precipitation (40-60%)

    • Some estimates:

      • DJF - 90% stratiform and 10% convective

      • MAM - 35% stratiform and 65% convective

      • JJA - 20% stratiform and 80% convective

      • SON - 35% stratiform and 65% convective


Types of precipitation focus on stratiform
Types of precipitation: focus on stratiform precipitation

Stratiform

Large variations in the vertical, small in the horizontal

Weak w, < 1 m s-1 (w < VT)

Precipitation growth during the “fall” of a precipitation particle

Convective

Less substantial variations in the vertical, large in the horizontal

Strong w, 5-50 m s-1

Time dependence

Evolution to stratiform


Conceptual picture of precipitation growth in a stratiform and b convective clouds
Conceptual picture of precipitation growth in (a) stratiform and (b) convective clouds

Quasi-steady state process, function of height

Fig. 6.1 from Houze

Time-dependent process, but also a function of height


Idealized stratiform cloud system and (b) convective clouds

10

Ice crystals

Snow

6 km

Height (km)

Aggregates

0.4 km

Rain

Melting layer:

Water-coated or spongy ice

4 km

0

0 2 4 6 8 10

Vertical variation of particle types within a nimbostratus stratiform cloud system

Mean diameter (mm)


Melting within stratiform precipitation produces the radar bright band

Ice crystals

Growth of pristine ice by deposition

Some growth by deposition, riming

Primary growth by aggregation

aggregates

melting

rain

Change in Z due to various processes (Wexler 1955), p. 200 in R&Y

Melting VT Shape Condensation Total

Snow to bright band +6 -1 +1.5 0 +6.5 dB

Bright band to rain +1 -6 -1.5 +0.5 -6 dB


Idealized radar profiles around the 0 c level
Idealized radar profiles around the 0 C level bright band

Growth by vapor deposition

Deposition, riming (?) and aggregation

Aggregation + melting

Conversion to raindrops,

breakup of aggregates (?)

Some notes:

Z for ice is lower than Z for snow of the same water content

because of difference in dielectric constant.

When all ice converts to raindrops, the particle concentration

is reduced due to increase fall speeds.



0548 bright band

MIPS


1247 bright band

MIPS


Variability in the bright band stratiform regions
Variability in the bright band (stratiform regions) bright band

sv

SNR

W

  • 0548 UTC

    • thick

    • enhanced SW layer above

    • uniform VT

  • 1247 UTC

    • thin

    • greater SW below

    • decreasing VT

0 C

0 C


Top panels: bright bandReflectivity shows the bright band, Doppler velocity shows the increase in fall speed as snow/aggregates melt to form rain drops.


Hurricane isaac
Hurricane Isaac bright band


Measured profiles of ice hydrometeors
Measured profiles of ice hydrometeors bright band

Fig. 6.3 from Houze. Ice particle concentration obtained from aircraft flights through nimbostratus in tropical MCSs over the Bay of Bengal.


Structure of a stratiform rainband, showing dynamical and microphysical processes. Fig. 6.8 from Houze (1993)


Numerical simulation design of precipitation processes in frontal stratiform precipitation. Fig. 6.9 from Houze


Results of a numerical simulation of precipitation processes in a frontal stratiform rainband. Each panel shows the rates of conversion for the process considered (10-4 g kg-1 s-1)


Conceptual model of the development of nimbostratus associated with deep convection. Fig. 6.11 from Houze

Fig. 6.10 Houze


Schematic of the precipitation mechanisms in a MCS. Solid arrows are hydrometeor trajectories. From Fig. 6.13 of Houze



Examples of a four different narrow cold frontal rainbands. The location of the cold front is shown. Note the different orientation of the smaller elements within the rainband. Fig. 11.28 of Houze


Hypothesized airflow along a cold frontal rainband, and the development of wave features due to horizontal shearing instability. (Fig. 11.30 of Houze).

Schematic of the relative airflow across two precipitation cores, and the gap between them, in a narrow cold frontal rainband. The airflow, represented as wind vectors, was inferred from Doppler radar. Fig. 11.29 from Houze.


Cloud structure, air motions, and precipitation mechanisms within cold frontal bands. This structure is derived from aircraft, Doppler radar, and other sources. Fig. 11.31 of Houze.


Schematic of clouds, precipitation, and thermal field of a warm frontal rainband as deduced from rawinsonde, aircraft and radar data. The region above the elevated warm front is convectively unstable (qe decreases with height). Fig. 11.38 of Houze.


UAH/NSSTC ARMOR 10/27/2006: 3-D View of light, stratiform warm frontal rainband as deduced from rawinsonde, aircraft and radar data. The region above the elevated warm front is convectively unstable (

Rain Rate

Plan view

125 km

Profile of liquid dependent on ice process/types

Polarimetric Hydrometeor ID

Radar Reflectivity

Vertical Cross-Section 300o

10

Height (km)

5

0

Dry Snow

Light. Rain

Drizzle

Melting Layer

Horiz.-oriented ice

Irreg. Ice

Wet Snow

Proprietary information, Walter A. Petersen, University of Alabama Huntsville


ARMOR: 27 October 2006 Bright band variability and precipitation

(RHI’s over MIPS wind profiler every 2-3 minutes)

+/- 500m oscillations in melting level height, and finally a rise with warm front!

DSD properties from combined profiler/radar retrieval




Stratiform precipitation within a midlatitude cyclone precipitation

Small ice crystals

Snow (1-2 mm)

large aggregates (5-10 mm)

bright band

large raindrops (2-3 mm)

small raindrops (1-2 mm)

time

Reflectivity factor measured by a vertically pointing X-band radar

Stratiform precipitation with both ice and water phase is common over large regions in both the tropics (mesoscale convective systems and tropical storms) and midlatitudes (within low pressure regions)

The bright band region could be especially problematic.




Vertically pointing Doppler radar measurements within a stratiform rain band

Reflectivity factor:

Bright band

Rain streaks

Doppler velocity

Fall speeds for snow vs. fall speeds for rain

Spectrum width

Low in snow (not much variation in fall speeds), high in rain (greater variation in fall speeds)


Reflectivity
Reflectivity stratiform rain band

Generating Cells

Dry Slot

Radial Velocity (vertical)

Spectrum Width


Reflectivity1
Reflectivity stratiform rain band

Generating Cells

Radial Velocity (vertical)


Precipitation Paths: Possible scenarios stratiform rain band

Precipitation

Stratiform rain system with bright band and large aggregates near the bright band (relatively common)

Shallow convective cloud, small drops (0.5 mm diameter)

Shallow convective cloud, large drops (e.g., the Hawaiian shallow clouds that develop raindrops to diameters of 5-8 mm; Rauber et al 1991).

Deep convective cloud with graupel, snow, aggregates, and rain

Item (4), with the addition of hail

Clouds without large precipitation

Stratocumulus clouds, between 0.2 and 0.8 km above sea level (ASL), with 0.2 mm drizzle droplets (common)

Cirrus clouds, between 8 and 12 km ASL, with ice crystals up to 1 mm in diameter (common)


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