Boyce, Robert E (1981): (Table 1) Electrical resistivity, sound velocity, thermal conductivity, density-porosity, and temperature at DSDP Hole 61-462 [dataset]. PANGAEA, https://doi.org/10.1594/PANGAEA.819954, Supplement to: Boyce, RE (1981): Electrical resistivity, sound velocity, thermal conductivity, density-porosity, and temperature, obtained by laboratory techniques and Well Logs: Site 462 in the Nauru Basin of the Pacific Ocean. In: Larson, RL; Schlanger, SO; et al. (eds.), Initial Reports of the Deep Sea Drilling Project (U.S. Govt. Printing Office), 61, 743-761, https://doi.org/10.2973/dsdp.proc.61.133.1981
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Abstract:
At Deep Sea Drilling Project (DSDP) Site 462, from mudline to 447 meters below the sea floor, Cenozoic nannofossil oozes and chalks have acoustic anisotropies such that horizontal sonic velocities are 0 to 2.5% faster than those in the vertical direction. In laminated chalk, anisotropy of 5% is typical, and in limestones, radiolarian oozes, porcellanites, and cherts, the anisotropies range from 4 to 13%. Middle Maestrichtian volcaniclastics from 447 meters to 560 meters below the sea floor have an acoustic anisotropy of 2 to 32%; 4 to 13% is typical. Basalt flows and sills occur between 560 meters and 1068 meters, and have no apparent anisotropy, but minor interbedded volcaniclastics have anisotropies from 0 to 20% (5% is typical). These volcaniclastics frequently have very small anisotropies, however, compared with the volcaniclastic sequence above the basalt section.
Data in cross-plots of the laboratory-measured compressional sound velocity versus wet-bulk density, wet-water content, and porosity of sediments and sedimentary rock typically lie between the equations derived by Wyllie et al. (1956) and Wood (1941); the Wyllie et al. (1956) equation has a fair fit with similar basalt velocity cross-plots. Crossplots of thermal conductivity and sound velocity indicate only a fair correlation. Cross-plots of thermal conductivity versus porosity, wet-water content, and wet-bulk density correlate well with equations derived by Maxwell (1904), Ratcliff (1960), Parasnis (1960), and Bullard and Day (1961). Electrical formation factor versus porosity for sediments and sedimentary rock agrees with the Archie (1942) equation, with m values of 2.6; for basalt, an m of about 2.1 is typical. Basalt pore-water resistivities do not appear to be greatly different from sea water. Formation factors are greater than those derived from equations in Maxwell (1904), Winsauer et al. (1952), Boyce (1968), and Kermabon et al. (1969). An "apparent interstitial water resistivity" (Rwa) curve was derived from the density and induction logs. This Rwa curve indicated an anomaly, at 393.5 to 396.5 meters, which could be interpreted as (1) 76% hydrocarbons, (2) relatively fresh pore water (1.8 per mil salinity), or (3) low-grain-density (2.2 g/cm**3) semi-lithified porcellanite-chert. Porcellanite-chert is the most plausible interpretation.
In situ temperatures measured by the Uyeda temperature probe were about 2 to 5°C (50%) higher than the equilibrium temperature (Lachenbruch and Brewer, 1959) extrapolated from two Gearhart-Owen continuous temperature logs; this discrepancy probably arises because the hole was washed out in this depth interval, so these extrapolated temperatures are probably not reliable. If one ignores all precautions as to temperature artifacts, then the equilibrium temperatures of the Gearhart-Owen temperature logs suggest that hydrothermal circulation is occurring in at least the upper 40 meters of the basalt section and heat is transferred by convection and not conduction. Hydrothermal circulation is probably not indicated, however, and the temperature anomalies probably result from excessive artificial cooling of the fractured basalt zones by circulation of water during drilling.
Project(s):
Deep Sea Drilling Project (DSDP)
Coverage:
Latitude: 7.237500 * Longitude: 165.030500
Date/Time Start: 1978-05-28T00:00:00 * Date/Time End: 1978-05-28T00:00:00
Minimum DEPTH, sediment/rock: 394.0 m * Maximum DEPTH, sediment/rock: 579.0 m
Event(s):
61-462 * Latitude: 7.237500 * Longitude: 165.030500 * Date/Time: 1978-05-28T00:00:00 * Elevation: -5181.0 m * Penetration: 617 m * Recovery: 386 m * Campaign: Leg61 * Basis: Glomar Challenger * Method/Device: Drilling/drill rig (DRILL) * Comment: 70 cores; 627.4 m cored; 0 m drilled; 61.5 % recovery
Comment:
Sediment depth is given in mbsf. ? = value uncertain; empty cells = no data. Porosity = (roo-g - roo-b)/(roo-g - roo-w), where roo-g is 2.7 and 2.4 g/cm**3 for sedimentary material and 3.0 g/cm**3 for basalt, roo-w = 1.03 g/cm**3, and roo-b = wet bulk density from density log. roo-g estimated from laboratory porosity-density measurements.
Parameter(s):
| # | Name | Short Name | Unit | Principal Investigator | Method/Device | Comment |
|---|---|---|---|---|---|---|
| 1 | DEPTH, sediment/rock | Depth sed | m | Geocode | ||
| 2 | Sample ID | Sample ID | Boyce, Robert E | |||
| 3 | Pressure | P | kg/cm2 | Boyce, Robert E | see reference(s) | Hydrostatic pressure = depth below sea level x 1.035 g/cm**3 |
| 4 | Salinity | Sal | Boyce, Robert E | see reference(s) | Interstitial water salinity is from shipboard determination on sedimentary samples, and these data are assumed to apply to the basalt section | |
| 5 | Temperature, in rock/sediment | t | °C | Boyce, Robert E | see reference(s) | Temperature is from second temperature log |
| 6 | Resistivity, electrical | Resist electr | Ohm m | Boyce, Robert E | see reference(s) | In situ; Interstitial water electrical resistivity is calculated from temperature and salinity based on data of Thomas et al. (1934) and then corrected for hydrostatic pressure by techniques formulated by Home and Frysinger (1963) |
| 7 | Hole Diameter | HD | in | Boyce, Robert E | see reference(s) | |
| 8 | Resistivity, electrical | Resist electr | Ohm m | Boyce, Robert E | see reference(s) | The hole fluid electrical resistivity; The hole fluid was sea water with a salinity of 35%, and its in situ resistivity was calculated by the same method as that for interstitial water resistivity in footnote e |
| 9 | Resistivity, electrical | Resist electr | Ohm m | Boyce, Robert E | see reference(s) | True formationelectrical resistivity; Corrected for borehole diameters and bed thickness and adjacent bed resistivity |
| 10 | Formation factor | F | Boyce, Robert E | see reference(s) | F = (Rt/Rw) | |
| 11 | Porosity, fractional | Poros frac | Boyce, Robert E | see reference(s) | Porosity = m rout(1/F), Sed. m = 2.6, Bas. m = 2.1 | |
| 12 | Density, wet bulk | WBD | g/cm3 | Boyce, Robert E | Gamma-ray attenuation porosity evaluator (GRAPE) | |
| 13 | Porosity | Poros | % vol | Boyce, Robert E | see reference(s) | roo-g = 3 |
| 14 | Porosity | Poros | % vol | Boyce, Robert E | see reference(s) | roo-g = 2.7 |
| 15 | Porosity | Poros | % vol | Boyce, Robert E | see reference(s) | roo-g = 2.6 |
| 16 | Porosity | Poros | % vol | Boyce, Robert E | see reference(s) | roo-g = 2.4 |
| 17 | Gamma ray | Gamma | gAPI | Boyce, Robert E | ||
| 18 | Lithology/composition/facies | Lithology | Boyce, Robert E |
License:
Creative Commons Attribution 3.0 Unported (CC-BY-3.0)
Size:
200 data points