Index properties measurements were made on one sample per section in the first 17 cores in Hole 1119B and below this on an average of three per core to the total depth in Hole 1119C. Index properties were determined by a gravimetric method (see "Physical Properties" in the "Explanatory Notes" chapter). Values of measured index properties (void ratio, porosity, water content, bulk density, and grain density) are presented in Table T14 (also in ASCII format). The properties show little variation downcore, indicating a fairly homogeneous section, with the few variations most likely corresponding to lithologic responses to climatic (glacial-interglacial) signals (Fig. F26).
The shipboard physical properties program at Site 1119 included nondestructive measurements of bulk density, magnetic susceptibility, and natural gamma-ray activity on whole sections of all cores using the multisensor track (MST) (Fig. F27). Magnetic susceptibility was measured at 4-cm intervals and at a high sensitivity (4-s measurement time) in all Site 1119 holes. Magnetic susceptibility is generally low but shows pronounced cyclicity. Extremely low values may be associated with voids. Gamma-ray attenuation porosity evaluator (GRAPE) bulk density measurements were made at 4-cm intervals at all Site 1119 holes. Cyclic increases and decreases in GRAPE density are most likely a result of varying lithologies caused by climatic (glacial-interglacial) fluctuations. A comparison of GRAPE density with the wet-bulk density determined from discrete samples shows general agreement, although overall GRAPE density values are lower than bulk density values obtained by index property measurements (Fig. F28). This may result from the fact that index properties sample preparation involves some water loss and that GRAPE density is measured in undrained cores. In Hole 1119B (0 to 150 mbsf), the wet-bulk density is consistently greater than the GRAPE density. Agreement between these two parameters occurs in the lower part of the section (>190 mbsf). Possible reasons for the discrepancy in the upper part of the core (<190 mbsf) include differences in the handling time of the cores, loss of fluids because of increased hydrostatic pressure with depth, and the use of different coring methods for the two sections. In the case of handling time, the time interval between splitting the core and the processing of samples tends to increase with core depth as a result of the backlog of accumulating core materials to be processed. As for the increasing pressure downhole, this factor was magnified by a high gas content in the core, and increased effects of gas expansion were observed in the deeper cores as they equilibrated to surface temperature and pressure conditions. This could have allowed more moisture loss, resulting in better agreement in the deeper cores. The upper part of the section was collected using the APC coring method, whereas the deeper part of the section was cored using the XCB method. It is generally accepted that the XCB method causes greater disturbance in the cored materials than the APC method. This factor could also have made a contribution to the differing moisture content estimates. Increased GRAPE densities between 430 and 436 mbsf suggest a significant lithologic change in this interval. The P-wave velocity measurements (PWL) were made at 4-cm intervals but gave poor results because of signal attenuation and sediment cracking resulting from high gas content (see "Organic Geochemistry"). PWL measurements were not collected after Section 181-1119B-3H-1 and for the entire Hole 1119C. Natural gamma-ray activity was measured with a 15-s count every 14 cm in Holes 1119B and 1119C.
Measurements of shear strength, using a mechanical vane, were made on split cores from Hole 1119B (Fig. F29). Samples were generally taken in fine-grained sediments at a resolution of one per section in Hole 1119B. No samples were taken from XCB cores. Increased sand content in the sediment results in lower shear strength values. Values range from 10 to 70 kPa (maximum value 67.5 kPa at 152 mbsf) and generally increase with depth. Low values may be associated with the presence of sand-rich intervals (see "Lithostratigraphy"). Two significant increases occur at 88 and 129 mbsf after intervals of gradually decreasing shear strength. Shear strength values for Hole 1119C were obtained using the Torvane method. These data correlate well with those from the vane shear results from Hole 1119B (Fig. F28).
Compressional-wave velocity was measured parallel and normal to the core axis on split cores from Hole 1119B using the digital sound velocimeter system. The measurements gave poor results because of signal attenuation and sediment cracking resulting from high gas content (see "Organic Geochemistry"), and, therefore, all the velocity measurements were rejected at Site 1119.
Four downhole temperature measurements with the Adara temperature tool were taken in Cores 181-1119B-4H, 7H, 10H, and 13H. Thermal conductivity was measured in cores where the Adara temperature tool was used, at an average of three or four per core for both Holes 1119B and 1119C. The Adara temperature tool yielded poor results at the site, which precluded the determination of heat flow. Downhole distribution of thermal conductivity at Holes 1119B and 1119C is shown in Figure F30. The data collected from cores from these two holes generally agree. The overall trend of the values measured is similar, but absolute values are generally higher in Hole 1119C.