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At least 1,297 records · Page 72
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NASA NTRS1977

Rayed craters on the moon and Mercury

Systems of bright rays are exhibited by many fresh craters on the moon and Mercury. Diameter/density distributions suggest that lunar-rayed craters represent the Class 1 craters, and that Mercurian rayed craters represent post-Caloris craters. Photogeological analyses of lunar imagery indicate that the ray systems are composed of finely divided material from the primary crater along with locally derived ejecta from secondary and tertiary craters. The primary ray material probably occurs in moderately thick (0.1-1 meter) deposits. The rate of darkening may depend more on the thickness of the ray material than on the rates of various darkening processes. Darkening rate may also be a function of crater size. It is observed that rays of craters more than 1 b.y. old remain bright, whereas those older than Class 1 generally fade to imperceptibility.

Allen, C. C.↗
NASA NTRS1977

Electromagnetic sounding of the moon using Apollo 16 and Lunokhod 2 surface magnetometer observations /preliminary results/

A technique of deep electromagnetic sounding of the moon using simultaneous magnetic-field measurements at two lunar surface sites is described. The method, used with the assumption that deep electrical conductivity is a function only of lunar radius, has the advantage of allowing calculation of the external driving field from two surface-site measurements only and therefore does not require data from a lunar orbiting satellite. A transient-response calculation is presented for the example of a magnetic-field discontinuity, measured simultaneously by Apollo 16 and Lunokhod 2 surface magnetometers.

Vanian, L. L.↗
NASA NTRS1978

The distortion of the moon due to convection

Numerical calculations of the dynamical ellipticity of the moon due to finite-amplitude solid-state convection indicate that convection could be the cause of the nonhydrostatic gravitational figure, but only if the lunar lithosphere is capable of resisting global scale deformation. Thus lithospheric inhomogeneities and surface loads could also contribute substantially to the disequilibrium of the gravity figure. The calculations also show that it is unlikely that the geometrical distortion is due to convection.

Cassen, P.↗
NASA NTRS1978

On the accelerations of the moon and sun, the constant of gravitation, and the origin of mountains

On the assumption of a constant value for the gravitational constant G, the lunar and solar tidal couples and the rate of change of angular velocity of the earth are recalculated on the basis of the improved values for the apparent accelerations of the moon and sun arrived at by Muller and Stephenson (1977). These new values are then used to derive general dynamical equations with a changing moment of inertia and changing G connecting the apparent accelerations to the lunar and solar couples. The effect of a changing G is considered, and a value of (dG/dt)/G = -3 times 10 to the -11th power per yr can be reconciled only weakly with the improved accelerations, especially for the case of linear friction. For quadratic friction the situation is more favorable. The new accelerations, however, are best reconciled with a nonchanging G, and certainly cannot be reconciled with a value of (dG/dt)/G = -6 times 10 to the -11th power per yr.

Lyttleton, R. A.↗
NASA NTRS1977

On the origin of the moon, with emphasis on bulk composition

A new analysis of altimetric, gravimetric, and seismological results, together with petrological and thermal history constraints, obtains an estimated Al2O3 content of 5.0%, 2.1 times chondritic. Hence the moon definitely has a refractory lithophile excess as well as an iron deficiency. In addition, the lunar surface is characterized by refractory siderophile depletions. The combination of these properties appears to require a previous stage of differentiation in a planetary body or bodies. Siderophile and chalcolphile depletions and dispersions in eucrites suggest that these bodies are not necessarily large. Possible mechanisms of lunar formation include impacting of a very large body into the earth; tidal disruption of sizeable differentiated planetesimals by the earth; and selective capture of differentiated planetesimal material by small moonlets. Each mechanism has its difficulties; the major unknown affecting all of them is the size distribution of planetesimals.

Kaula, W. M.↗
NASA NTRS1977

The effects of target characteristics on fresh crater morphology - Preliminary results for the moon and Mercury

The results are reported of an analysis of the characteristics of fresh crater samples occurring on the two major geologic units on the moon (maria and highlands) and on Mercury (smooth plains and cratered terrain). In particular, the onset diameters and abundances of central peaks and terraces are examined and compared for both geologic units on each planet in order to detect any variations that might be due to geologic unit characteristics. The analysis of lunar crater characteristics is based on information provided in the LPL Catalog of Lunar Craters of Wood and Andersson (1977). The Mercurian data set utilized is related to a program involving the cataloguing of Mercurian craters visible in Mariner 10 photography. It is concluded that the characteristics of the substrate have exerted a measurable influence on the occurrence of central peaks, terraces, and scallops in flash crater samples. Therefore, in order to compare the morphologic characteristics of fresh crater populations between planets, an analysis of possible substrate-related differences must first be undertaken for each planet under consideration. It is suggested that large variations in gravity do not produce major variations in crater wall failure.

Cintala, M. J.↗
NASA NTRS1977

Size-dependence in the shape of fresh impact craters on the moon

The transition from small simple craters to large complex or modified craters is characterized by eleven changes in the shape of fresh lunar craters which occur within a diameter range of 10 to 30 km. In the present paper, seven ratio-level variations - those of rim-crest diameter with depth, rim height, flank width, rimwall slope, floor diameter, circularity, and rim-crest evenness - are defined for fresh-appearing craters from the new Apollo data and are expressed mathematically where practicable. These relations constitute a shape model for interpreting fresh craters on the moon. The size dependent changes reflect the occurrence of central peaks, rimwall terraces, and a flat floor within craters measuring 10 to 20 km in diameter.

Pike, R. J.↗
NASA NTRS1975

Evolution of the moon between 4.6 and 3.3 AE

A model of lunar evolution is proposed. At 4.6 AE an outer shell 60-100 km thick of an initially homogeneous moon was totally molten following accretion. 'Highland basalt' represents remnants of the chilled crust of this molten layer and, therefore, the mean lunar composition. Melt from the partially molten region below the outer shell intruded into it, enriching it in FeO, SiO2, radiogenic, and trivalent trace LIL (large ion lithop) elements. Fractional crystallization of the outer shell produced toward its base a mafic cumulate zone less than 40 km thick, the upper 60 km being anorthosite. The radiogenic elements concentrated together with dense residual melt in the upper parts pf the mafic cumulate zone. Between 4.6 and 4.3 AE a second differentiation led to localized enrichment from below of radiogenic elements in the plagioclase-rich, high-Mg/Mg + Fe residuum below the outer 100-km-thick shell. Melting at these enriched sites at about 4.0 AE produced to KREEP basalts. Later melting at sites of radiogenic element enrichment in the outer 100-km-thick shell produced the mare basalts.

Hollister, L. S.↗
NASA NTRS1975

Photogeological, geophysical, and geochemical data on the east side of the moon

Correlations between Apollo orbital data and geologic data for eight map provinces are reported for a region centered on the east limb of the moon (50 deg N to 50 deg S and 50 deg E to 140 deg E). The appearance of the provinces is described, and the basins in or near the region are assigned relative ages. The western (nearside) part of the region averages about 3 km lower in elevation than the eastern (farside) part, according to laser altimeter measurements which are used to make geologic cross sections. Gravity data correlate with most geologic provinces and the surface profiles made by the laser altimeter and lunar sounder. The distribution of concentration ratios of Al/Si and Mg/Si as well as the distribution of relatively low natural radioactivity are considered.

El-Baz, F.↗
NASA NTRS1975

Shock effects from a large impact on the moon

The paper calculates the shock and shear deformation-induced internal energy distribution associated with a major basin-forming hypervelocity meteorite impact on the moon. The Hageman and Walsh formulation of the axisymmetric two-dimensional conservation equations in finite difference form is used, and the flow field induced upon impact of an iron meteorite traveling at 15 km/sec with a gabbroic anorthosite lunar crust is calculated for sequential time steps over a grid of hoop-shaped zones fixed in space. If an energy of 5 times 10 to the 32nd power ergs for the projectile energy is required to excavate a basin of Imbrium size, than a flow field of approximately 210 km in radius approximately 19 seconds after impact is indicated. The meteorite residue, the melt, and the ejecta are discussed, and the results are compared with the Gault and Heitowit (1963) formulation.

Okeefe, J. D.↗
NASA NTRS1978

The puzzling moons of Mars

Viking Orbiter observations of Phobos and Deimos are presented with attention to physical dimension and surface features. Both satellites are approximately 1.4 times as long as they are wide; Phobos having a length of 27 km, while Deimos is half that size. In addition, both satellites are tidally locked, as is earth's moon, and are held together by cohesive forces as well as by gravity. Phobos and Deimos are both heavily cratered, and Phobos has deep (30 m) grooves in the vicinity of its largest crater, Stickney; indicating surface fracturing under meteorite impact. The craters on Deimos are largely filled with a fine-grained substance, probably crater ejecta.

Veverka, J.↗
NASA NTRS1978

Fission origin of the moon - Cause and timing

A new scenario is offered for the origin of the moon. It is assumed that the earth formed initially with about the maximum amount of angular momentum consistent with dynamical stability. This state is approximated by the secularly unstable Maclaurin spheroids (highly flattened hamburger-shaped bodies). It is shown that the earth cannot depart from this state at a reasonable rate as long as its viscosity is in the range of liquid rock. Since core formation supplies about 1600 kJ/kg, the earth will not leave this state until core formation is complete. When cooling produces a rise in viscosity, the earth will necessarily evolve along a path which is approximated by the Riemann ellipsoids (which have rapid internal motion). The evolution is toward a Jacobi ellipsoid, but it is intercepted by the development of a third-harmonic (pear-shaped) instability, which is catastrophic and leads to fission. The process of fission itself may be fundamentally analogous to the breaking of a wave in water. We cannot exclude the possibility that some other planets evolved similarly.

Okeefe, J. A.↗
NASA NTRS1978

Lunar Seismology: the Internal Structure of the Moon

The direct P and S wave arrival times are the primary data set that can be measured on the seismograms of natural lunar seismic events. Polarization filtering techniques allow the enhancement of secondary body wave arrivals and record curves to identify the secondary phases and deduce structural information. Finally, shear wave amplitude vs. distance curves yield information on the location and magnitude of seismic velocity gradients in the interior. The results of these analyses show that the moon appears to have a two-layer crust at all four seismic stations: a 20 km upper crust that seems to be constant at all sites and a lower crust that is 40 km thick at stations 12 and 14 (mare), 55 + or - 10 km at station 16 (highland), and tentatively either 40 km or 70 km at station 15. The lower mantle extends from 480 km to at least 1100 km depth which is the maximum depth of penetration of all but a few seismic waves used as data. No definitive evidence for or against a lunar core exists.

Goins, N. R.↗
NASA NTRS1978

Earth rotation and polar motion from laser ranging to the moon and artificial satellites

Earth-based laser ranging to artificial satellites and to the moon is considered as a technique for monitoring the Earth's polar motion and diurnal rotation. The kinematics of Earth rotation as related to laser ranging is outlined. The current status of laser ranging as regards its measuring capabilities is reviewed. The relative merits of artificial satellite and lunar laser ranging are pointed out. It appears that multistation combined artificial satellite and lunar laser ranging is likely to ultimately meet a 0.002 arcseconds in pole position and 0.1 msec in UT1 daily precision requirement.

Aardoom, L.↗
NASA NTRS1978

Moon-magnetosphere interaction and estimates of possible lunar core size

It is shown that estimates of the size of a possible lunar core are negligibly affected by currents due to a directed plasma flux toward the moon. A theory for the compression of an induced lunar dipole by an incoming sub-Alfvenic flux of cold plasma is presented for the time-independent case where the external magnetic field, induced dipole moment, and plasma velocity vector are all aligned, and it is demonstrated that, at very long time periods, effects due to the inertia of an incoming flow of cold plasma can be ignored. A theory for time-dependent fluctuations in a stationary plasma is modified to include the effects of incoming flux.

Goldstein, B. E.↗
NASA NTRS1979

A review of earth-based radar mapping of the moon

Lunar radar mappings carried out in the late 1960s and 1970s have provided several valuable insights into lunar surface processes. These radar mappings used the delay-Doppler technique and needed the narrow antenna beams now available with large radio telescopes. Two-element radar interferometers have provided resolution of the delay-Doppler ambiguity at meter wavelengths and provided topographic information at centimeter wavelengths. These techniques have provided high resolution lunar radar maps at 3.8-cm, 70-cm, and 7.5-m wavelengths, a set of wavelengths which span the window available for earth-based radar mapping of the moon. These radar maps have been used along with other earth-based and Apollo orbital measurements to define surface units. The radar maps and these other data can describe physical properties such as small-scale blockiness and surface chemistry.

Thompson, T. W.↗
NASA NTRS1979

The magnetic fields of Mercury, Mars, and moon

Mariner observations have shown a significant global magnetic field at Mercury with a dipole moment at a tilt of 14 + or - 5 deg relative to the normal of the orbit plane. A presently active dynamo is the most likely origin for the planet's magnetic field. Limited evidence for an intrinsic magnetic field on Mars was obtained by USSR spacecraft in 1971 and 1974. The Martian magnetic field, if it exists, may result from either remanent magnetism or an active dynamo. On the moon, local magnetic fields have been detected by the Apollo and Lunokhod missions, but no global correlation of the steady state values has been noted.

Ness, N. F.↗