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Quick soundvelocity measurements by an improved pulsesuperposition methodThe "elastic constants" of a crystal are referred to a Cartesian coordinate system which has a definite relation to the crystal axes. In determining these constants from sound-velocity mea~urements at least as many measurements must be made as there are constants to be determined a?~ in general m~re than o.ne propagation direction will be used. Thus, in order to relate the m:asu:ed velocIties t.o the :lastlc properties of the crystal one needs to solve the equation of motion for the directIOn under ~onsl~erat~on, and to k?ow the transformation equations that relate the elastic properties along the propagatIOn directIOn to the desired elastic constants. In this paper a perturbation solution to the equation of motion is presented as w.ell a~ the transformation equations for triclinic and all higher symmetry crystal classes. Also pre~ented ~re slm~hfica tions that will be of use in designing experiments and reducing the data. Several mistakes III prevIOusly published work are corrected. 4

The rate of production of sea water droplets by bubble bursting at the ocean surface is very difficult to measure directly. Laboratory simulations are also difficult. However, the surface flux can be inferred from measurements of the rate of change of aerosol densities and changes in the height of the marine boundary layer. Data from CEWCOM‐78 have been analyzed to produce the aerosol surface flux volume spectrum from 0.8 to 15 μm radius at a wind speed of 9 m s−1. Using this flux spectrum and equilibrium aerosol spectra from JASIN, flux spectra are calculated for wind speeds from 6 to 18 m s−1.

The dissipation rate of turbulent kinetic energy, E, and the temperature structure function parameter, C& have been measured over water from the near surface (Z = 3 m) to the top of the boundary layer. The near surface values of E and C; were used to calculate the velocity and temperature Monin Obukhov scaling parameters u. and 7',. The data collected during unstable lapse rates were used to evaluate the feasibility of extrapolating the values of s and C+ as a function of height with empirical scaling formulae. The dissipation rate scaling formula of Wyngaard et al. (1971a) gave a good fit to an average of the E data for Z < 0.8 Zi. In the surface layer the scaling formula of Wyngaard et al. (1971b) disagreed with the C+ values by as much as SOY& This disagreement is due to an unexpected reduction in the measured values of C$ for Z < 30 m. At this point it is not clear if the discrepancy is a unique property of the marine boundary layer or if it is simply some unknown instrumental or analytical problem. The mixed layer scaling results were similar to the overland results of Kaimal et al. (1976).

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