Hole 1116A (RCB):
9°51.934´S, 151°34.508´E; 1851.3 mbsl
0158.90 mbsf cored; 32.61 m recovered (21%)
Site 1116 is located on the southern flank of Moresby Seamount, 8 km south of Site 1114, within a tilted block bounded by two normal faults that each offset the basement by >1 km to the south-southwest. The objectives for this site were to characterize the early rift sediments and the seamount basement (which was not reached).
Very low surface porosity (~30%), and high bulk density (~2.15 g/cm3), sonic velocity (2.22.8 km/s), and thermal conductivity (1.02.2 W/(mK) values, suggest that 7001000 m of the section has been removed by faulting and/or erosion. This is consistent with the lack of a Quaternary and uppermost Pliocene section, as well as the seismic stratigraphy.
The recovered section is dominated by Pliocene indurated sandstones alternating with siltstones/claystones. The sandstones are fine to medium, occasionally coarse grained, and display parallel, wavy, and convolute laminations, which indicate they originated from turbidity currents in a near-source slope setting. A paraconglomerate is at 3463 mbsf. The sandstones below this are subarkosic with a calcareous matrix. Measured CaCO3 contents are <5%. Some thick-bedded, reverse-graded sandstones with occasional intraformational rip-up clasts were deposited from high-density turbidity currents. However, normal grading and lamination in some siltstones/sandstones also indicate deposition by low-concentration turbidity or bottom currents. The matrix-supported conglomerates, interbedded with sandstones and siltstones, comprise relatively unaltered, mainly angular clasts and are interpreted as debris-flow deposits.
Benthic foraminifers indicate middle bathyal paleowater depths (5002000 m), with inner neritic (<50 m) benthic foraminifers redeposited within turbidite beds. The N20/N21 boundary (3.35 Ma) occurs between 104 and 128 mbsf, and the minimum age of 1.95 Ma at the surface yields a minimum sedimentation rate of 70 m/m.y. Burrows are either abundant or relatively depleted, suggesting alternating poorly and well oxygenated subseafloor conditions; within both cases abundant detrital organic matter input and a mostly terrigeneous source are indicated by C/N ratios.
The orientations of the subhorizontal maximum axes of the ellipsoids of magnetic susceptibility (corrected for bedding dip and core orientation) below 100 mbsf indicate northeast-southwest or northwest-southeastdirected paleocurrents during sedimentation.
The sources of clastics are little-altered basic extrusive rocks of mainly calc-alkaline affinities, probably derived from the Miocene Tobriand Arc, but also include silicic extrusives, shallow-water bioclasts, metamorphics, and serpentinite. The serpentinite, rare chromite, and some of the gabbro and diabase grains probably have an ophiolitic origin (PaleoceneEocene Papuan Ultramafic Belt?).
The upper 100 m of the section shows abundant evidence of synsedimentary deformations, including folding and low-angle extensional faulting typical of gravity-driven processes. The bedding dips <10%, except for fold limbs where it is up to 50%. Common dewatering and fluidization features were possibly seismically triggered. Faults and scaly fabrics are within a narrow zone between 100 and 120 mbsf. They include steep strike-slip and 25%- to 55%-dipping pure normal faults. Below the fault zone, beds dip ~15%, consistent with the dip of seismic reflectors.
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