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inferred pyroxene and plagioclase microcrystals did not show obvious alteration features or boundary-enhanced microstructures, which support the pseudomorphization of pyroxenes by plagioclases during alteration events (e.g., 206-1256d-19r-1 [piece 3, 4-5 cm] and 3r-2 [piece 5, 16-23 cm]).
we collected 187 lithic fragments from roughly perpendicular to subparallel, northwest-dipping normal faults and thrusts. faults are mostly unsampled. a small amount of altered matrix is common to the largest boulder-size pieces.
a few lenses of altered rock (phyllosilicates, carbonates, organic matter, and pyrite) are present in the unconsolidated matrix of piece 206-1256b-12r-2 (ca. 37 cm). the altered matrix is not rimmed by an erosional syncline or anticline. in this interval, the large diameter (>3 cm) and thin slices of hyaloclastite (white layers) of piece 206-1256b-14r-1 (ca. 50 cm) are covered by a fine ( < 1 cm) to coarse-grained to granular matrix (yellow-brown layers) containing quartz, hematite, and pyrite. the hyaloclastite segments occasionally are still bounded by the original massive drapes of unweathered basalts. volcaniclastics are not present.
large shards of altered fine-grained to microcrystalline glass were found within a poorly defined yellow-brown matrix with no obvious pebbles or rock fragments of our rock types. in the red-brown matrix of piece 206-1256b-21r-2 (ca. 60 cm), the shales have angular and planar, large-diameter (up to 1 cm) reactivated intragranular microcracks.
basalt—hosted rocks. we identified two types of basalts in hole 1256c: a basaltic facies, in which primary minerals include relatively large volumes of leucite, and a granitic facies, in which primary minerals include an in situ pyroxene-phenocryst assemblage. we identified other basalts in the core of hole 1256d that are host to feldspar and in situ pyroxene phenocrysts and a primary matrix composed of clinopyroxene. these intervals are described below.
thermal features formed in these rocks are interpreted as reflecting magmatic activity during cooling. dikes, sills, and flow-dominated structures (e.g., kyanite gneiss, coarsened gneiss, sinitic gneiss, mixed oxides, antigorite, and hornblende-hornblende gneiss) are present in some intervals. they are interpreted as intragranular cooling features because they cut and/or reactivate the underlying late to postmagmatic glass and alteration features.
healed intracrystalline microcracks are also present in many intervals. especially, long (several millimeters up to a few centimeters in length) and curved microcracks cut through the rocks and intergrow with alteration layers and diagenetic features. the microcracks are interpreted to be laterally propagating cooling-induced faults occurring in the rock at different times according to their locations and dip.
angular unconformities are commonly recognized in some intervals. these unconformities typically show angular to poorly weathered, planar, basal to near-vertical structures cut by planar or rootlike variscite, anhydrite, greenschist, chlorite, or olive greenschist sills, diabase, and andesite dykes. the angular unconformities commonly have a folded margin.
sediments associated with late-stage igneous activity recorded in the odp core include all of the above-described structures, along with exhalative diagenetic features like breccias, spheroidal conglomerates, vesiculated sandstones, and basic alteration products like kyanite and anhydrite.
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