Polarization Radar - Department of Atmospheric Sciences

Transcript Polarization Radar - Department of Atmospheric Sciences

Dual Polarization Radars

Long-standing Problems

Distinguishing, ice and liquid phases of precipitation using radar Identifying specific hydrometeor populations, such as hail or supercooled water Quantifying, rain, snow and hailfall rates using radar.

Multi-Parameter Measurements

(Measurements of two or more parameters of the radar signal) Standard Doppler radar (Z HH , V r ,  ) Polarization radar (signals of two different polarizations are processed): Many parameters can be derived * Note notation: Z HH Transmitted at horizontal polarization Received at horizontal polarization

Literature

Zrnic, D. S., and A. Ryzhkov: Polarimetry for Weather Service Radars. BAMS, 1999, 389-406 Doviak and Zrnić, 1993: Doppler Radar and Weather Observations. Academic Press.

Bringi and Chandrasekar, 2001: Polarimetric Doppler Weather Radar. Cambridge University Press.

Vivekanandan, Zrnić, Ellis, Oye, Ryzhkov, Straka, 1999: Cloud microphysical retrieval using S-band dual-polarization radar measurements.

Bull. Amer. Meteor. Soc.

, 381-388.

Straka, Zrnić, Ryzhkov, 2000: Bulk hydrometeor classification and quantification using polarimetric radar data: Synthesis and Relations.

J. Appl. Meteor.

, 1341-1372.

http://www.nssl.noaa.gov/~schuur/radar.html

Outline

- Polarization of electromagnetic waves - Linear polarimetric observables (Z DR , LDR, Φ DP (K DP ), ρ HV ,) - Types of dual-polarization radars today Research and Applications: - Hydrometeor classification - Rainfall estimates

Electromagnetic Waves Linear Polarization

E E (Doviak and Zrnić, 1993) http://www.nssl.noaa.gov/~schuur/radar.html

Circular Polarization

E Practical use of circular polarization: Tracking aircraft in precipitation.

Light to moderate rain: removal of a large portion (e.g. 99%) of the precipitation echo (transmitted right-hand circular polarized waves become, when scattered from small spherical drops, left-hand polarized).

Scattering may be Rayleigh or Mie

Scattering cross section for spherical drops assuming Rayleigh scattering     5 4

6 (spherical drops with D small compared to λ) - Theoretical and experimental work has been done relating particles scattering cross section to other shapes, sizes and mixture of phases.

Terminology

Copolar power

: Power received at the same polarization as the transmitted power (e.g. transmit horizontal, receive horizontal, transmit vertical, receive vertical)

Cross-polar power

: Power received at the opposite polarization as the transmitted power (e.g. transmit horizontal, receive vertical, transmit vertical, receive horizontal)

Two ways in which hydrometeors affect polarization measurements:

Backscatter effects

by particles located within the radar resolution volume

Propagation effects

by particles located between the radar resolution volume and the radar

Backscatter effects

by particles located within the radar resolution volume Six basic backscatter variables: 1. Reflectivity factor for horizontal polarization Z HH 2. The ratio of the reflected power (or reflectivity factor) at horizontal/vertical polarization (P HH /P VV called the Differential Reflectivity (Z DR ).

or Z HH /Z VV ) 3. The ratio of cross-polar power to copolar power (PVH/PHH) called the Linear Depolarization Ratio (L DR )

Backscatter effects

by particles located within the radar resolution volume Six basic backscatter variables: Phase difference in H and V caused by backscattering 4. The correlation coefficient between copolar horizontally and vertically polarized echo signals 

HV e i

 5. The complex correlation coefficient between copolar horizontal and cross-polar (horizontal transmission) echo E(V HH *V HV ) 6. The complex correlation coefficient between copolar vertical and cross-polar (vertical transmission) echo E(V HH *V HV )

Propagation effects

by particles located between the radar resolution volume and the radar 1. Attenuation of the horizontal component 2. Attenuation of the vertical component 3. Depolarization 4. Differential phase shift (phase difference in returned signal for the two polarizations)  DP

Differential Reflectivity Z

Z

[dB] = 10 log(

z HH z VV

)

4 mm 3.7 mm 2.9 mm – Depends on axis ratio oblate: ZDR > 0 prolate: ZDR < 0 – For drops: Z DR ~ drop size (0 - 4 dB) 2.7 mm 1.8 mm 1.4 mm (Pruppacher and Klett, 1997)

Z

(cont.) Z

= 10 log(

z HH z VV

)

– For ice crystals: • columns (1 – 4 dB) • plates, dendrites (2 – 6 dB) (Pruppacher and Klett, 1997)

Z

(cont.) Z

= 10 log (

z HH z VV

)

– For hail: (-1 – 0.5 dB) – For graupel: (-0.5 – 1 dB) – For snow: (0 – 1 dB) (Hobbs, 1974) (Pruppacher and Klett, 1997)

Z

(cont.)

• Independent of calibration • Independent of concentration (but can depend on how the concentration is distributed among various sizes • Is affected by propagation effects (e.g. attenuation)

Linear Depolarization Ratio LDR LDR [dB] = 10 log( z

H V z HH

)

4 mm 3.7 mm 2.9 mm • Spheroidal hydrometeors with their major/minor axis aligned or orthogonal to the electric field of the wave: LDR dB • Detects tumbling, wobbling, canting angles, phase and irregular shaped hydrometeors: • large rain drops (> -25 dB) • Hail, hail and rain mixtures (-20 - -10 dB) • wet snow (-13 - -18 dB) (Pruppacher and Klett 1997)

LDR (cont.)

• Susceptible to noise (cross-polar signal is 2-3 orders of magnitude smaller than copolar signal) • Independent of radar calibration • Independent of number concentration • Lowest observable values : -30 dB (S-Pol), -34 dB (Chill)

Differential Propagation Phase Φ

Φ

[deg.]= Φ

– Φ

VV Φ HH , Φ VV : cumulative differential phase shift for the total round trip between radar and resolution volume).

Φ HH , Φ VV = differential phase shift upon backscatter + differential phase shift along the propagation path

Φ

(cont.) Φ

= Φ

– Φ

VV • Statistically isotropic particles produce similar phase shifts for horizontally and vertically polarized waves.

• Statistically anisotropic particles produce different phase shifts for horizontally and vertically polarized waves.

• A volume with oblate hydrometeors (large rain, ice crystals): horizontal polarized wave propagates more slowly than vertically polarized wave => larger phase shifts (Φ HH ) per unit length => Φ DP increases.

(Doviak and Zrnić, 1993)

Φ

(cont.)

(Doviak and Zrnić, 1993)

Φ

(cont.)

Specific Differential Propagation Phase K

Φ

(r

) - Φ

(r

) K

[deg/km] = 2(r

– r

)

• Independent of receiver/transmitter calibration • Independent of attenuation • Less sensitive to variations of size distributions (compared to Z) • Immune to particle beam blocking

Correlation Coefficient ρ

HV Correlation between horizontally and vertically polarized weather signals Physical occurrence of decorrelation: Horizontal and vertical backscatter fields, caused by each particle in the resolution volume, do not vary simultaneously.

(Doviak and Zrnić, 1993)

ρ

(cont.)

ρ

(cont.)

• Influenced by particle mixture (e.g. rain/hail mixture) • Influenced by the differential phase shifts Φ HH, Φ VV (e.g. oscillation of large drops) • Influenced by the distributions of eccentricities (e.g. oscillation of large drops) • Influenced by canting angles (large drops) • Influenced by irregular particle shapes (e.g. hail, graupel)

ρ

(cont.)

• Independent of radar calibration • Independent of hydrometeor concentration • Immune to propagation effects

Polarization Radars Today

S-Pol (NCAR)

• NSF funded • S-band dual polarization Doppler radar • Highly mobile (fits in 6 sea containers) • Antenna diameter 8.5 m • Beam width 0.91 deg • Range resolution 150 m (Photos: Scott Ellis)

• NSF funded

Chill (CSU)

• S-band dual polarization Doppler radar • Antenna diameter 8.5 m • Beam width (3 dB) 1.1 deg • Range resolution 50, 75, 150 m

Dual-polarized Radar Systems

(Polarization-agile/dual-receiver systems) S-Pol Chill (Bringi and Chandrasekar, 2001)

Koun WSR-88D Radar

(NSSL Norman, OK) • Polarimetric upgrade of NEXRAD radar, completed in March 2002 • Simultaneous/hybrid transmission scheme

Wyoming King Air Cloud Radar

(UW) • K-band • Dual/single polarization Doppler radar • Beam width 0.4 – 0.8 deg (depending on antenna type) • Antenna configurations down, side, up

NOAA Developments

• Millimeter-wave cloud radar (MMCR) to study the effects of clouds on climate and climate change • Ground-based cloud radar for remote icing detection (GRIDS) to provide automated warnings of icing conditions • Mobile X-band dual-polarization Doppler radar (Hydro Radar) to study storm dynamics, boundary layer turbulence and ocean-surface characteristics

DLR

• C-band • First meteorological radar system designed to measure time-series of “instantaneous” scattering matrices

Polarization variables from Cimmaron radar, which is located north of the squall line Attenuation Note KDP vs Z estimate of rain

radar

Z DR  DP Z V r LDR

Future Radar Screen?

 HV

Hydrometeor classification

Vivekanandan, Zrnić, Ellis, Oye, Ryzhkov, Straka, 1999: Cloud microphysical retrieval using S-band dual-polarization radar measurements.

Bull. Amer. Meteor. Soc.

, 381-388.

• Algorithm runs in real time • Based on a fuzzy logic method

Overall Design

Real time application Fuzzy logic technique 5 observed and computed polarimetric variables Temperature profile Hydrometeor type Result: For each volume element one particle type

All Hydrometeor Types

Z = 47 dBZ Z DR = 1.2 dB LDR = -24 rain

Fuzzification

Reflectivity 1 P= hail 0 35 45 55 65 Z DR P= 1 0 -1 0 1 2 LDR 1 Rain Hail 0.8

0.2

1 P= 0.5

Sum= 2.3

0 0.1

0.3

0 -30 -25 -20 -15

Results

Other Algorithms

Precursor: Hard boundaries Successor: neuro-fuzzy system (combination of neural network and fuzzy logic) The performance of a fuzzy logic classifier depends critically on the membership functions. A neuro-fuzzy system learns from data and can adjust the membership functions.

Rainfall Estimation

Attempt to solve the inverse electromagnetic problem of obtaining – resolution volume averaged – rainrates from backscatterer measurements such as Z, ZDR and KDP together with an underlying rain model.

One Z-R relationship used by WSR-88D radars: R(Z) = 0.017 Z 0.714

• Requires accurate knowledge of the radar constant • Prone to errors in absolute calibration

R(Z, Z

) Algorithm R = c

Z

h a 1

10

0.1 b 1 Z DR

[mm/h]

• Z DR can be measured accurately without being affected by absolute calibration errors Table from Bringi and Chandrasekar, 2001

R(K

) Algorithm R = 40.5 (K

)

0.85

[mm/h]

• Valid for 10 cm wavelength and the Pruppacher and Beard model for the raindrop shape •Unaffected by absolute calibration errors and attenuation • Unbiased if rain is mixed with spherical hail • KDP is relative noisy at low rainrates • Estimated over finite path (trade off between accuracy and range resolution)

Standard Deviation K

DP (Bringi and Chandrasekar, 2001)

R(K

, Z

) Algorithm R = c

K

DP a 3

10

0.1 b 3 Z DR

[mm/h]

• Z DR can be measured accurately without being affected by absolute calibration errors Table from Bringi and Chandrasekar, 2001

Advantages

• Distinction of rain from other types of hydrometeors possible (important step prior to rainfall estimates) • Estimation of rainfall rates not only on the ground (vertical structure gives insight in precipitation processes)