Recorded presentation5.2
Lidar-radar measurements of snowfall
Edwin W. Eloranta, Univ. of Wisconsin, Madison, WI
Aerodynamic flow around gauges and the horizontal transport of windblown snow along the surface produce errors in snowfall measuremets. Comparisons between various snow gauges with and without wind shields show as much as as a factor of two difference between measurements(Yang et al., 1999). These problems are particularly significant in the high Arctic where snowfall amount are very low and blowing snow is frequent.
This paper describes a lidar-radar based technique to measure the downward flux of snow at an altitude of ~100m.
When particles are small compared to the wavelength, radar reflectivity is proportional to the number of snowflakes times the square of the mass of the average snowflake. For particles large compared to the wavelength, the lidar extinction cross section is equal to two times the number of snowflakes times the projected average area of the snowflakes. Donovan and Lammeren(2001) show that the ratio of radar to lidar cross sections can be used to define an effective-diameter-prime, which is proportional to the fourth root of the average mass-squared over the average projected area of the snowflakes. If one assumes a crystal shape this can be converted into an effective-diameter which is the average mass over the average area of the flakes. Multiplying the lidar measured projected area times the effective-diameter yields the mass of the particles. The product of this mass and the radar measured vertical velocity then provides the vertical flux of water.
In past work we have tested this measurement approach with data acquired in the high Arctic at Eureka, Canada(80 N,86 W). Measurements from the University of Wisconsin High Spectral Resolution Lidar and the NOAA 35 GHz cloud radar were used to compute the time-integrated flux of water at 100 m above the surface. This result was compared with Nipper gauge measurements of snowfall acquired as part of the Eureka weather station record. Best agreement was achieved when the crystals where assumed to be bullet-rosettes. However, because the conversion from effective-diameter-prime to effective-diameter is dependent on the ratio of crystal thickness to diameter, the results are strongly dependent on the assumed crystal morphology.
In this paper we describe a lidar-radar measurement approach which derives the crystal aspect ratio through a comparison of the effective-diameter-prime and the radar measured fall velocity. This provides an aspect ratio measurement for each sample volume and removes the need to assume an ice crystal shape. Particle thickness is assumed to be related to particle diameter by a power law (Auer and Veal, 1970). For the purpose of computing radar and lidar cross sections and the particle fall velocity, we assume a prolate spheroid shape for the particles. Fall velocities are related to particle projected area and particle mass using the power-law formulation due to Mitchell(1994).
The lidar-radar results show reasonable agreement with the Eureka station record. Limitations of the method include the need to time-average the radar Doppler velocity data to reduce the influence of air motion on the measured particle fall velocities. In addition, when cloud water droplets are present along with snowflakes at the measurement level the lidar-radar retrievals of aspect ratio fail. In the future it may be possible to use the spectrum of the radar Doppler measurement to separate particle velocity from the air motion, Shupe(2008).
References:
Yang, D., B. Goodison, J. Metcalfe, V. Golubev, R. Bates, T. Pangburn, and C. Hanson: 1998, Accuracy of the NWS 8" Standard Nonrecording precipitation Gauge: Results and application of WMO intercomparison, J. Atmos. Tech., 15, 54-68.
Donovan, D, and A. van Lammeren: 2001, Cloud effective particle size and water content profile retrievals using combined lidar and radar observations 1. Theory and examples, J. Geophy. Res., 106, 274250-27448.
Auer, A, D. Veal: 1970,The dimension of Ice Crystals in Natural Clouds, J. Atmos. Sci., 27, 919-926.
Mitchell, D.: 1996, The use of Mass- and Area-Dimensional Power Laws for Determining Precipitation Particle Terminal Velocities, J. Atmos. Sci., 53, 1710-1722.
Shupe, M., P. Kollias, M. Poellot, and E. Eloranta: 2008, On Deriving vertical Air Motions from Cloud Radar Doppler Spectra, J. Atmos. & Oceanic Tech. 25, 547-557
Session 5, Lidar Application Studies in The Boundary Layer and Lower Troposphere - II
Tuesday, 13 January 2009, 3:30 PM-5:00 PM, Room 122A
Previous paper Next paper