Physical Properties of Sediment Recovered on Deep Sea Drilling Project Leg 68 with the Hydraulic Piston Corer

Mayer, Larry A.

doi:10.2973/dsdp.proc.68.111.1982

Cited by 14 publications

(15 citation statements)

References 18 publications

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“…Although porosities are high in Unit II and Subunits IIIA and IIIB, especially considering porosities of sediments at equivalent pressures at Sites 645 and 646 (Fig. 10), similar highporosity siliceous sediments at comparable sub-bottom depths have been documented at Deep Sea Drilling Project (DSDP) sites in the equatorial Pacific (Keller and Bennett, 1973;Mayer, 1982), Bering Sea (Lee, 1973), and Norwegian Sea (Talwani, Udintsev, et al, 1976). The high porosity of these sediments was attributed to the structural traits of siliceous microfossils that produce an open sediment framework.…”

Section: Discussion Compaction Patterns At Baffin Bay and Labrador Sementioning

confidence: 68%

Patterns of Sediment Compaction at Ocean Drilling Program Sites 645, 646, and 647, Baffin Bay and Labrador Sea

Busch¹

1989

Proceedings of the Ocean Drilling Program

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With several exceptions, porosity and density measurements of sediments cored at Site 645 in Baffin Bay and Sites 646 and 647 in the Labrador Sea reveal compaction patterns typical of terrigenous sediments. Deviation from standard porosity trends is greatest at depths shallower than 350 meters below seafloor (mbsf). This depth range contains the greatest variability in porosity at the individual sites and the largest differences between the Leg 105 sites and other terrigenous sediment sections. Porosity variation in this range is attributed primarily to differences in sediment texture and composition. At greater depths, pressure is the dominant factor influencing compaction, and the patterns are more uniform. Sediments at Sites 645 and 646 parallel typical terrigenous sediment porosity profiles. The more rapid decrease of porosity at Site 647 probably reflects the greater age and diagenetic alteration of these sediments. Comparisons of porosity profiles for the three sites are based on laboratory-measured porosities corrected for sediment expansion. At Site 646, the expansion correction procedure yields a porosity profile that closely matches a profile based on porosities estimated from the borehole sonic log.

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Section: Discussion Compaction Patterns At Baffin Bay and Labrador Sementioning

confidence: 68%

Patterns of Sediment Compaction at Ocean Drilling Program Sites 645, 646, and 647, Baffin Bay and Labrador Sea

Busch¹

1989

Proceedings of the Ocean Drilling Program

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“…The data obtained from Sites 588, 590, and 592 show little change in compressional wave velocity over the top 300 m of the sediment column. In their physical properties study, Wilkens and Langseth (1983) report that seismic velocity exhibited the least variation with depth of any of the parameters measured; Mayer (1979Mayer ( , 1982 arrived at a similar conclusion. Fluctuations in this elastic property remained small across large depth intervals, even as other physical properties changed significantly.…”

Section: Acoustic Velocitymentioning

confidence: 77%

“…Mayer (1982) has addressed the issue of sediment disturbance and has found specimen quality to be very high when the HPC has functioned properly. HPC refusal began to occur during this cruise at coring depths near 250 m, coincident with the appearance of the stiffer chalks, and a newly developed extended core barrel (XCB) was utilized for subsequent core retrieval.…”

Section: Grape Analysesmentioning

confidence: 99%

Physical Properties of Calcareous Sediments from the Southwest Pacific

Morin¹

1986

Initial Reports of the Deep Sea Drilling Project

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The extensive hydraulic piston coring activity on Leg 90 provided hundreds of meters of good quality sediment from which to conduct a comprehensive physical properties examination of nannofossil ooze and chalk. Most sites exhibit a well-defined transitional zone between the soft ooze and the indurated chalk, and a clear correlation is established between the onset of this region and sharp increases in sediment shear strength. Distinct increases in the values of compressional velocity and thermal conductivity across the ooze-to-chalk transformation are less evident. In a few instances, the porosity-versus-depth profiles depict zones where sediment porosity remains relatively constant across substantial depth intervals. Porosity is seemingly unaffected by large increases in overburden pressure, and no significant compaction occurs across several hundred meters of the sediment column. This behavior is attributed to a combination of several environmental factors. It is postulated that remarkably high sedimentation rates, a high diagenetic potential, and, perhaps, an appropriate grain size distribution all have had some relative influence in promoting sediment rigidity and retarding compaction.

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“…The structural attributes of sili ceous microfossils result in an open sediment framework, pro ducing the anomalously low bulk density and high water con tent and porosity. Siliceous sediments with similarly anomalous properties at sub-bottom depths comparable to those at Site 647 were observed in Deep Sea Drilling Project sites in the equato rial Pacific Mayer, 1982). In Hole 647A, low wet-bulk density is also associated with mean grain densities that are as low as 2.32 g/cm 3 at 213.44 mbsf (Table 9), resulting from the abundance of biogenic silica.…”

Section: Index Propertiesmentioning

confidence: 92%

Site 647

1987

Proceedings of the Ocean Drilling Program

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Core recovery (%): 62Srivastava, S. P., Arthur, M., Clement, B., et al., 1987. Proc, Init. Repts. (Pt. A) Principal results: Holes 647A and 647B, Site 647, were drilled in a water depth of 3858.5 m, at 53°19.876'N, 45°15.717'W, in the southern Labrador Sea. The total depth of penetration was 736 mbsf; average recovery during rotary drilling at Hole 647A was 62% and during APC coring at Hole 647B, 90%. Four major sedimentary units were encountered between the seafloor and 699 mbsf, and basalt was re covered from 699 to 736 mbsf. The lithologic units are as follows: Lithologic Unit I (Cores 105-647A-1R to 105-647A-12R; 105-647B-1H to 105-647B-11H) 0-116 mbsf. Age: late Pliocene to Holo cene. Description: consists of interbedded gray to light brownish gray silty clays, clayey muds, and clayey silts containing highly varia ble amounts of biogenic carbonate (foraminifers, nannofossils) to a maximum of 40%-50%. Lithologies are interbedded on a scale of from 10 cm to 3 m, having both sharp and gradational contacts. Silty clays, clayey muds, and clayey silts are structureless to color mottled. Foraminifer-nannofossil silty clays or clayey silts are homo geneous, but pockets within or at the tops of beds are enriched in foraminifers; the tops of such thin beds have sharp contacts with overlying beds. Detrital (nonbiogenic) carbonate occurs as dissemi nated silt-sized grains (as much as 50%) and as concentrations of as much as 75% in thinly laminated silty clay to clayey silt layers. Some of these layers have sharp bases and exhibit grading. All facies except the laminated detricarbonate silty clay layers contain variable amounts of sand-and gravel-sized material to cobble size. The upper 675 SITE 647 50 m of Unit I are coarser grained than the lower part, but no sys tematic trend to the biogenic content exists. However, intervals con taining gravel and those relatively rich in biogenic constituents alter nate in a cyclical but irregular pattern.Lithologic Unit II (Cores 105-647A-13R to 105-647A-14R) 116.0-135.4 mbsf. Age: early Miocene to late Miocene. Description: pri marily mottled olive-yellow to yellowish brown silty mud, clay, and nannofossil clay (Subunit IIA, 116-119 mbsf) and olive-yellow to grayish green silica-bearing (as much as 25%) clays lacking calcare ous nannofossils (Subunit IIB, 119-135.4 mbsf). Subunit IIA con tains quartz silt (as much as 25%) and scattered iron/manganese micronodules that increase in abundance toward the base; the sediment is bioturbated to homogeneous. Subunit IIB is marked by diatomand spicule-bearing silty clay; biogenic silica (as much as 15%) con tents increase toward the base. Dark-gray bands of iron/manganese micronodules occur in the upper part, and larger iron/manganese nodules appear near the base of the subunit. Subunit IIB is biotur bated and mottled.Lithologic Lithologic Unit IV (Cores 105-647A-56R to 105-647A-71R) 530.3-699.0 mbsf. Age: middle Eocene to early Eocene. Description: pre dominantly greenish gray claystone and foraminifer-nannofossil-bearing claystone with...

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Physical Properties of Sediment Recovered on Deep Sea Drilling Project Leg 68 with the Hydraulic Piston Corer

Cited by 14 publications

References 18 publications

Patterns of Sediment Compaction at Ocean Drilling Program Sites 645, 646, and 647, Baffin Bay and Labrador Sea

Patterns of Sediment Compaction at Ocean Drilling Program Sites 645, 646, and 647, Baffin Bay and Labrador Sea

Physical Properties of Calcareous Sediments from the Southwest Pacific

Site 647

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