1. Robin Hogan, Chris Westbrook University of Reading Lin Tian NASA Goddard Space Flight Center Phil Brown Met Office The importance of ice particle shape and orientation for spaceborne radar retrievals

2. Introduction and overview To interpret 94-GHz radar reflectivity in ice clouds we need –Particle mass: Rayleigh scattering up to ~0.5 microns: Z mass 2 –Particle shape: non-Rayleigh scattering above ~0.5 microns, Z also depends on the dimension of the particle in the direction of propagation of the radiation Traditional approach: –Ice particles scatter as spheres (use Mie theory) –Diameter equal to the maximum dimension of the true particle –Refractive index of a homogeneous mixture of ice and air New observations to test and improve this assumption: –Dual-wavelength radar and simultaneous in-situ measurements –Differential reflectivity and simultaneous in-situ measurements Consequences: –Up to 5-dB error in interpretted reflectivity –Up to a factor of 5 overestimate in the IWC of the thickest clouds

3. Dual-wavelength ratio comparison NASA ER-2 aircraft in tropical cirrus 10 GHz, 3 cm 94 GHz, 3.2 mm 10 GHz, 3 cm 94 GHz, 3.2 mm Difference Error 1: constant 5-dB overestimate of Rayleigh- scattering reflectivity Error 2: large overestimate in the dual-wavelength ratio, or the Mie effect

4. Characterizing particle size An image measured by aircraft can be approximated by a... Sphere (but which diameter do we use?) Spheroid (oblate or prolate?) Note: D max D long D mean =(D long +D short )/2

5. Error 1: Rayleigh Z overestimate Brown and Francis (1995) proposed mass[kg]=0.0185 D mean [m] 1.9 –Appropriate for aggregates which dominate most ice clouds –Rayleigh reflectivity Z mass 2 –Good agreement between simultaneous aircraft measurements of Z found by Hogan et al (2006) But most aircraft data world-wide characterized by maximum particle dimension D max –This particle has D max = 1.24 D mean –If D max used in Brown and Francis relationship, mass will be 50% too high –Z will be too high by 126% or 3.6 dB –Explains large part of ER-2 discrepancy

6. Particle shape We propose ice is modelled as oblate spheroids rather than spheres –Korolev and Isaac (2003) found typical aspect ratio =D short /D long of 0.6-0.65 –Aggregate modelling by Westbrook et al. (2004) found a value of 0.65 Randomly oriented in aircraft probe: Horizontally oriented in free fall:

7. Error 2: Non-Rayleigh overestimate Spheroid Sphere Transmitted wave Sphere: returns from opposite sides of particle out of phase: cancellation Spheroid: returns from opposite sides not out of phase: higher Z

8. Independent verification: Z dr A scanning polarized radar measures differential reflectivity, defined as: Z dr = 10log 10 (Z h /Z v ) Solid-ice sphere Solid-ice oblate spheroid Sphere: 30% ice, 70% air D short /D long : Dependent on both aspect ratio and density (or ice fraction) If ice particles were spherical, Z dr would be zero!

9. Reflectivity agrees well, provided Brown & Francis mass used with D mean Differential reflectivity agrees reasonably well for oblate spheroids Chilbolton 10-cm radar + UK aircraft

10. Z dr statistics One month of data from a 35- GHz (8-mm wavelength) radar at 45° elevation –Around 75% of ice clouds sampled have Z dr < 1 dB, and even more for clouds colder than -15°C –This supports the model of oblate spheroids For clouds warmer than -15° C, much higher Z dr is possible –Case studies suggest that this is due to high-density pristine plates and dendrites in mixed-phase conditions (Hogan et al. 2002, 2003; Field et al. 2004)

11. Consequences for IWC retrievals Empirical formulas derived from aircraft will be affected, as well as any algorithm using radar: Raw aircraft dataEmpirical IWC(Z,T) fit Spheres with D =D max Hogan et al. (2006) fit New spheroids Radar reflectivity ~5 dB higher with spheroids Retrieved IWC can be out by a factor of 5 using spheres with diameter D max Note: the mass of the particles in these three examples are the same