(Table 1) Electrical resistivity, sound velocity, thermal conductivity, density-porosity, and temperature at DSDP Hole 61-462

At Deep Sea Drilling Project (DSDP) Site 462, from mudline to 447 meters below the sea floor, Cenozoic nannofossil oozes and chalks have acoustic anisotropies such that horizontal sonic velocities are 0 to 2.5% faster than those in the vertical direction. In laminated chalk, anisotropy of 5% is typical, and in limestones, radiolarian oozes, porcellanites, and cherts, the anisotropies range from 4 to 13%. Middle Maestrichtian volcaniclastics from 447 meters to 560 meters below the sea floor have an acoustic anisotropy of 2 to 32%; 4 to 13% is typical. Basalt flows and sills occur between 560 meters and 1068 meters, and have no apparent anisotropy, but minor interbedded volcaniclastics have anisotropies from 0 to 20% (5% is typical). These volcaniclastics frequently have very small anisotropies, however, compared with the volcaniclastic sequence above the basalt section. Data in cross-plots of the laboratory-measured compressional sound velocity versus wet-bulk density, wet-water content, and porosity of sediments and sedimentary rock typically lie between the equations derived by Wyllie et al. (1956) and Wood (1941); the Wyllie et al. (1956) equation has a fair fit with similar basalt velocity cross-plots. Crossplots of thermal conductivity and sound velocity indicate only a fair correlation. Cross-plots of thermal conductivity versus porosity, wet-water content, and wet-bulk density correlate well with equations derived by Maxwell (1904), Ratcliff (1960), Parasnis (1960), and Bullard and Day (1961). Electrical formation factor versus porosity for sediments and sedimentary rock agrees with the Archie (1942) equation, with m values of 2.6; for basalt, an m of about 2.1 is typical. Basalt pore-water resistivities do not appear to be greatly different from sea water. Formation factors are greater than those derived from equations in Maxwell (1904), Winsauer et al. (1952), Boyce (1968), and Kermabon et al. (1969). An "apparent interstitial water resistivity" (Rwa) curve was derived from the density and induction logs. This Rwa curve indicated an anomaly, at 393.5 to 396.5 meters, which could be interpreted as (1) 76% hydrocarbons, (2) relatively fresh pore water (1.8 per mil salinity), or (3) low-grain-density (2.2 g/cm**3) semi-lithified porcellanite-chert. Porcellanite-chert is the most plausible interpretation. In situ temperatures measured by the Uyeda temperature probe were about 2 to 5°C (50%) higher than the equilibrium temperature (Lachenbruch and Brewer, 1959) extrapolated from two Gearhart-Owen continuous temperature logs; this discrepancy probably arises because the hole was washed out in this depth interval, so these extrapolated temperatures are probably not reliable. If one ignores all precautions as to temperature artifacts, then the equilibrium temperatures of the Gearhart-Owen temperature logs suggest that hydrothermal circulation is occurring in at least the upper 40 meters of the basalt section and heat is transferred by convection and not conduction. Hydrothermal circulation is probably not indicated, however, and the temperature anomalies probably result from excessive artificial cooling of the fractured basalt zones by circulation of water during drilling.在深海钻探计划（Deep Sea Drilling Project, DSDP）462号站位，从海底面至海底以下447米的地层中，新生代超微化石软泥与白垩岩呈现声波各向异性特征：其水平声波速度较垂直方向高出0~2.5%。层理发育的白垩岩各向异性典型值为5%；而灰岩、放射虫软泥、瓷岩及燧石的各向异性比值介于4%~13%之间。海底以下447米至560米处的上马斯特里赫特期火山碎屑岩，声波各向异性为2%~32%，典型值为4%~13%。海底以下560米至1068米段发育玄武岩流与岩床，无明显声波各向异性，但其中夹层的火山碎屑岩各向异性为0~20%（典型值5%）。不过相较于玄武岩段之上的火山碎屑岩序列，这类夹层火山碎屑岩的各向异性通常极小。 实验室测得的沉积物与沉积岩纵波速度与湿体密度、湿基含水量、孔隙度的交会图数据，通常落在Wyllie等人（1956）与Wood（1941）推导的公式区间内；Wyllie等人（1956）的公式与玄武岩纵波速度交会图的拟合程度尚可。热导率与声波速度的交会图仅显示中等程度的相关性。热导率与孔隙度、湿基含水量、湿体密度的交会图，则与Maxwell（1904）、Ratcliff（1960）、Parasnis（1960）及Bullard与Day（1961）推导的公式吻合度较高。沉积物与沉积岩的地层电系数与孔隙度的关系符合Archie（1942）公式，其m值为2.6；玄武岩的m值典型值约为2.1。玄武岩孔隙水电阻率与海水并无显著差异。实测地层电系数高于Maxwell（1904）、Winsauer等人（1952）、Boyce（1968）及Kermabon等人（1969）公式的计算结果。研究人员基于密度测井与感应测井推导得到了“视孔隙水电阻率（Rwa）”曲线。该曲线在393.5米至396.5米深度段显示异常，可被解释为以下三种情况之一：(1) 含76%的烃类，(2) 低盐度孔隙水（盐度1.8‰），或(3) 颗粒密度为2.2 g/cm³的半固结瓷岩-燧石。其中，瓷岩-燧石是最合理的解释。 利用上田温度探头测得的原位温度，较基于两段吉尔哈特-欧文连续温度测井外推得到的平衡温度（Lachenbruch与Brewer, 1959）高出约2~5℃，温差幅度达50%。该偏差大概率源于该深度段的井眼垮塌，因此这些外推得到的平衡温度并不可靠。若忽略所有针对温度伪影的防控措施，则吉尔哈特-欧文温度测井得到的平衡温度表明，玄武岩段至少在上部40米范围内存在热液循环，热量通过对流而非传导进行传递。然而，热液循环大概率并不存在，该温度异常可能源于钻井过程中水体循环对破碎玄武岩带的过度人工冷却。