Temperatures were measured as a function time and depth in a borehole before and after it had been filled with water. The hole is 25 cm in diameter, 340 m deep, and effectively sealed from influx of ground water. The measurements reveal that: (1) Temperature differences between the air‐filled hole and the water‐filled hole (after dissipation of the water injection disturbance) do not exceed 0.05°C at the same depth. (2) Temperatures in the water‐filled hole exhibit oscillations at all depths where temperature increases downward but are stable at the bottom and near the surface where temperature decreases with depth. (3) The temperature oscillations have periods ranging from several minutes to several hours. (4) The amplitudes of the oscillations are several hundredths of a degree, and are roughly proportional to the geothermal gradient near the point of measurement, thus suggesting that the size of cells or eddies are rather constant and that the distance of water movement is no more than several times the inner diameter of the casing. (5) No oscillations were detected in the air‐filled hole, but because the time constants of the instrument are long in an air‐filled hole, the possibility of short period oscillations cannot be excluded.

Salt used for deicing the streets near Rochester, New York, has increased the chloride concentration in Irondequoit Bay at least fivefold during the past two decades. During the winter of 1969-70 the quantity and salinity of the dense runoff that accumulated on the bottom of the bay was sufficient to prevent complete vertical mixing of the bay during the spring. Comparison with 1939 conditions indicates that the period of summer stratification has been prolonged a month by the density gradient imposed by the salt runoff.

The time of the first arrival of seismic waves generated by explosions at the Nevada Test Site and recorded along a 300‐km line southeastward through Kingman, Arizona, is expressed as T0 = Δ/5.2, T1 = 0.34 + Δ/6.15, and T2 = 5.82 + Δ/7.81, where time is in seconds and the shot‐detector distance (Δ) is in kilometers. Assuming constant velocities for the layers, the thicknesses are H0 = 1.7 km, H1 = 26.7 km, and H0 + H1 ≐ 28 km (below a 1‐km datum). The average Bouguer anomaly is about −120 milligals, and the average elevation is about 1.1 km. Seismograms were examined for P waves indicating the presence of other discontinuities within and below the H2 layer, but the separation between seismic stations was too great to establish the presence of such discontinuities. A questionable alignment of weak arrivals following the T2 refraction time by less than 1 second may indicate the presence of a discontinuity below 28 km. Fair alignments of strong second arrivals in the range 200 to 400 km might be interpreted as direct P waves or channel waves in the H1 layer.

Sample No. Assigned sample number indicates that measurement was made in our laboratory. No sample number means that conductivity measurement was obtained from literature or from another source. See Remarks column. Mineral. Chemical formulae are generally for pure end members and are the formulae to which the theoretical densities (column 7) correspond. For many samples, the chemical composition is poorly known. Theoretical density. Data from Robie, and others (1966). They refer to idealized formula given under "Mineral". Temperature. The temperature at which the conductivity measurement was made. Pressure. The axial pressure on the sample. Remarks. Wards, sample from Wards Natural Science Establishment, Inc.; USNM, sample from U.S. National Museum: their number follows in parentheses. X-ray, indicates that composition was verified by X-ray diffraction. Heavy reliance has been placed on Clark's (1966) tabulation, and in some cases the original sources have not been checked. Wards, Joplin, Mo. Light gray, xls <0.1 an. Wards. Dover Cliff, England. Dark gray, xls <0.1 an. Wards. Virgin Valley, Nev. White, xls <0.1 mm. Ratcliffe (1959) from curve K versus T. Feldspar group Or t hod as e KAlSi.O..

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