MST measurements were conducted on whole-round sections of cores from each hole to obtain wet bulk density, compressional (P-wave) ultrasonic velocity, and magnetic susceptibility (see "Explanatory Notes" chapter, this volume). Natural gamma radiation was measured below 75 mbsf for a comparison with results from in situ logging (see "Downhole Logging" section, this chapter). Similar to Site 1076, many core sections from this site showed mechanical disturbance, probably because of degassing processes during core retrieval (see "Lithostratigraphy" section, this chapter).
Index properties (gravimetric density) measurements were made on one or two samples (volume = ~10 cm3) per working-half section on all cores (see "Explanatory Notes" chapter, this volume). Method C was utilized at this site.
Ultrasonic compressional (P-wave) velocities and undrained vane-shear measurements were made at a resolution of one or two samples per section. For the discrete P-wave pulse-transmission experiments, the digital sediment velocimeter (DSV) and the modified Hamilton Frame transducer systems were used.
The sampling rate for ultrasonic compressional wave velocity, GRAPE density (Fig. 24), and magnetic susceptibility (Fig. 25A) was 2 cm for the upper 75 m and was changed to 4 cm below 75 mbsf. MST data are included on CD-ROM (back pocket, this volume). At this depth, natural gamma radiation measurements were incorporated in the MST measurements, with a sampling period of 30 s at 4-cm resolution (Fig. 25B). Magnetic susceptibility and natural gamma radiation show some similarity in their profiles (Fig. 25A and (Fig. 25B, respectively), which may be attributed to higher proportions of magnetic particles at higher clay contents primarily monitored with NGR measurements (see "Lithostratigraphy" and "Downhole Logging" sections, this chapter). GRAPE density shows a good general correlation with discrete wet bulk density data (Fig. 24A-D). All MST core logs reveal pronounced cycles in physical properties and will, after thorough editing, provide high-resolution proxy information for fast temporal changes of sediment composition and environmental conditions. Compressional velocities were disregarded because of instrumental problems with the MST P-wave sensors (see "Physical Properties" section, "Site 1076" chapter, this volume).
Since the near-continuous velocity profile recorded with the MST had to be disregarded because of instrumental problems, only discrete velocity measurements are available. Velocities range between 1450 and 1555 m/s (Fig. 26). Discrete velocity measurements were conducted with the DSV system down to 35 mbsf, and then a switch was made to the Hamilton Frame (Fig. 26). The ultrasonic signals were highly attenuated below 100 mbsf. Discrete velocity values show larger scatter within the upper 35 m but reveal little variation below. The significant increase in velocities at 35 mbsf coincides with the change from the DSV to the Hamilton Frame system. This indicated that measurements with the DSV could not be carried out in this type of clay-rich sediment without affecting the mechanical integrity of the sediment between the transducers. Furthermore, only velocity measurements with the Hamilton Frame were made, also avoiding calibration problems between the two systems.
Results of discrete measurements of wet bulk density, porosity, and moisture content are presented in Fig. 27A, Fig. 27B, and Fig. 27C, respectively (also see Table 14). The density values vary within a narrow range between 1200 and 1350 kg/m3, indicating a very homogenous composition of the sediment (see "Lithostratigraphy" section, this chapter). A trend to higher values indicates compaction. Porosity decreases from 88% in the top section to 81% at 200 mbsf.
The thermal conductivity profile at Hole 1077A was measured by inserting a single probe in every second core section (see "Explanatory Notes" chapter, this volume). The values reveal significant scatter throughout the hole with decreasing values of even higher scatter toward the bottom (Fig. 25C).
In Hole 1077A, the Adara tool was deployed to measure formation temperature. A preliminary analysis provided five data points, which were used to estimate a geothermal gradient of 57°C/km, but further analyses will be required to confirm this result.
An undrained vane-shear measurement was performed in the bottom part of each core section. The profile shows a gradual increase of shear-strength values from the top to 115 mbsf (Fig. 25D). Because of the differential pressure that built up in the core liners during degassing, core integrity was more affected close to the top and bottom of each core. Accordingly, shear strength shows relative minima at the end of the cores. Maximum values probably represent undisturbed or less disturbed sections. From maximum values, an average increase in shear strength may be derived, which could be attributed to compaction.