All cores from Holes 897D and 899B were drilled using the rotary core barrel (RGB). Therefore, these cores were not oriented with respect to north. A total of 69 minicore samples (each with diameter 2.5 cm, length 2.2 cm) were taken from Holes 899B (36) and 897D (33) using a water-cooled nonmagnetic drill bit attached to a standard drill press. The samples were taken from long and continuous pieces of core sections so as to exclude those that had flipped over inside the drilling pipe, thus ensuring that the inclinations of the samples were not disturbed. The depth, freshness, color, and the general appearance of each sample were carefully registered. This sampling procedure facilitated the process of comparing the paleomagnetic results of individual samples with the corresponding core photographs and assessing the validity of the paleomagnetic results in a reliable manner. After splitting individual pieces of the core, ODP workers follow the same convention in handling rotary cores as for an oriented piston core (Fig. 3). Magnetic measurements were performed mainly with a 2G cryogenic magnetometer and a Schonstedt spinner magnetometer in the paleomagnetic laboratory at the University of California at Santa Cruz, but a few samples were measured during the cruise with Schonstedt and Molspin equipment. As the shipboard measurements revealed that these peridotites are highly susceptible to a magnetic field, subsequent shore-based demagnetization experiments were done in a zero-field paleomagnetic laboratory using Schonstedt equipment and a customized thermal demagnetization oven. For each sample, a vector plot of the directions of the magnetization during progressive demagnetization was analyzed to obtain the characteristic component (ChRM) and its polarity. Magnetic components, linear in three-dimensional space, were determined by fitting least-squares lines to segments of the vector demagnetization plots or by using "principal component analysis" methods (Zijderveld, 1967; Kirschvink, 1980). Bulk magnetic susceptibility and anisotropy of magnetic susceptibility (AMS) were measured using a Kappabridge KLY-2 (Geofyzika Brno). The susceptibility tensor (Kij) of each sample was calculated from the measurements in 15 positions. Several samples were subjected to 20-mT demagnetization with tumbling alternating field (AF) demagnetizer prior to AMS measurement in order to remove the scatter due presumably to AMS dependent on natural remanent magnetization (NRM). To avoid potential problems associated with heating (Rochette et al., 1992), the AMS measurement was completed before any thermal demagnetization experiments were conducted.