By A. J. Chisholm, Marianne English (auth.)
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N 27 JUNE 1967 WIND -10 COMPONENT 0 +10 STORM TO RELATIVE +20 8 ~6 >- I til2 I 0 6 4 HORIZONTAL / RADAR- 69 km 8 DISTANCE 10 12 ( km) FIG. 48. Schematic airflow in the plane of storm motion, 27 June 1967. The storm airflow enters on the downwind side of the storm, tilting slightly upwind to the storm top. Since the storm is in the early part of a mature stage, no outflow has been depicted. 6 --' ~4 >- LH I w2 I ~ STORM MOTION ~ 0 10 20 km FIG. 47. PPI sections at 1659 MST 27 June 1967, at elevation angles from 0°-5°.
I t consists of one large cell (supercell) which propagates continuously to the right of the mea n winds. The radar echo very often contains a hook echo near cloud base height. 2. The multicell storm. I t consists of several cells which are laterally a ligned. Discrete propagation occurs on t he right flank. The individual cells move through the storm complex a nd dissipate on the left flank. JU NE 1967 1538 - 1819 MST 5 HAIL PLOT 10 15 km R = RAIN ONLY X = NO RAI N, NO HAIL 0 : HAIL OF UNKNOWN SI ZE I = SHOT SIZE HA IL 2 = PEA SIZE HA I L 3 = GR APE SIZE HAI L 4 = WALN UT SIZE HAI L 5 = GOL FBALL S IZ E HAIL z, 18 19 MST F I G.
42. Radiosonde sounding for 1219 MST 29 June 1967. The dot-dashed line indicates a moist adiabatic parcel trajectory using representative cloud base conditions. Note the warm frontal inversion at 380 mb. Since the completion of the original analytical work which is reported in this study, considerable work on severe storms has ensued both in Alberta and Colorado. In this regard the work of Marwitz (1972a, b, c) is of particular note. Utilizing radar chaff as a tracer of airflow, Marwitz (1972a, c) obtained vertical velocities and horizontal motions within the WER of two severe storms in Colorado.