Logging data are measurements of physical properties of the formation surrounding a borehole, acquired in situ after completion of coring (wireline logging) or during drilling (Logging-While-Drilling, LWD). The range of data (resistivity, gamma radiation, velocity, density, borehole images,…) in any hole depends on the scientific objectives and operational constraints.

Logging data are measurements of physical properties of the formation surrounding a borehole, acquired in situ after completion of coring (wireline logging) or during drilling (Logging-While-Drilling, LWD). The range of data (resistivity, gamma radiation, velocity, density, borehole images,…) in any hole depends on the scientific objectives and operational constraints.

Logging data are measurements of physical properties of the formation surrounding a borehole, acquired in situ after completion of coring (wireline logging) or during drilling (Logging-While-Drilling, LWD). The range of data (resistivity, gamma radiation, velocity, density, borehole images,…) in any hole depends on the scientific objectives and operational constraints.

Recent measurements of in situ subseafloor pore pressure in sediment ponds on the flank of the Mid‐Atlantic Ridge using a Pop Up Pore Pressure Instrument have provided important information regarding fluid exchange processes at the seafloor as well as in situ estimates of physical properties of marine sediments. The in situ pore pressure recordings of 4–5 days duration contain three distinct components. The early part of the record is dominated by the decay of a pressure pulse associated with probe penetration. The rate of decay of this pulse is used to estimate in situ permeabilities, which range from 3.1 × 10−16 m2 to 6.5 × 10−15 m2. The recording also exhibits a low‐amplitude oscillation that is associated with tidal pressure variation on the seafloor. A study based on Biot's theory shows that amplitudes and phases of tidally induced pore pressure oscillations are determined by both the frame compressibility and the permeability of the sediments, and thus the oscillation components are used to estimate these parameters. The frame compressibilities and the permeabilities estimated from tidal oscillations range from 1.2 × 10−8 Pa−1 to 4.1 × 10−8 Pa−1 and from 1.1 × 10−15 m2 to 4.8 × 10−15 m2, respectively. Laboratory‐measured permeabilities range from 7.6 × 10−16 m1 to 1.2 × 10−15 m2. Permeabilities determined by these three methods are comparable. The third component is the ambient equilibrium pore pressure. Negative pore pressure gradients were identified on all deployments. When combined with the permeabilities of the sediments the estimated average rates of drawdown of water through the sedimentary layers in the ponds are 2–7 mm/yr. The pore pressure gradient near the seafloor can be used to construct a pore pressure profile through the sediment. Extrapolated pore pressure at the top of the basement is about 80 kPa (0.8 bar) below the hydrostatic pressure.

A few characteristics dominate the bulk physical properties of the sedimentary and igneous formations recovered in the Japan Sea on ODP Legs 127 and 128.The sediments above the opal-A/opal-CT boundary have high porosities over a large interval, with associated low wet-bulk densities and acoustic velocities; some of the detailed features in the uppermost sediments appear to correlate from site to site.The high porosities and general degree of underconsolidation are typical of sediments rich in biogenic silica.The diagenetic transformation from opal-A to opal-CT has a considerable effect on the sediment physical properties and serves as a widespread seismic and thermal marker horizon.The physical properties above and below the boundary are distinctly different.Finally, the interbedded igneous and sedimentary units give rise to strongly layered reflective sequences.The igneous units are highly altered, and the degree of alteration, as expressed through the loss on ignition, significantly affects the physical properties; the density and velocity are lower when alteration products such as clay or zeolite are present.

Research Article| September 01, 1982 A summary of Cenozoic tectonic history along the IPOD Japan Trench transect ROLAND VON HUENE; ROLAND VON HUENE 1U.S. Geological Survey, Menlo Park, California 94025 Search for other works by this author on: GSW Google Scholar MARCUS LANGSETH; MARCUS LANGSETH 2Lamont-Doherty Geological Observatory, Palisades, New York 10964 Search for other works by this author on: GSW Google Scholar NORIYUKI NASU; NORIYUKI NASU 3Ocean Research Institute, University of Tokyo, Tokyo, Japan Search for other works by this author on: GSW Google Scholar HAKUYU OKADA HAKUYU OKADA 4Geoscience Institute, Shizuoka University, Shizuoka, Japan Search for other works by this author on: GSW Google Scholar GSA Bulletin (1982) 93 (9): 829–846. https://doi.org/10.1130/0016-7606(1982)93<829:ASOCTH>2.0.CO;2 Article history first online: 01 Jun 2017 Cite View This Citation Add to Citation Manager Share Icon Share Facebook Twitter LinkedIn MailTo Tools Icon Tools Get Permissions Search Site Citation ROLAND VON HUENE, MARCUS LANGSETH, NORIYUKI NASU, HAKUYU OKADA; A summary of Cenozoic tectonic history along the IPOD Japan Trench transect. GSA Bulletin 1982;; 93 (9): 829–846. doi: https://doi.org/10.1130/0016-7606(1982)93<829:ASOCTH>2.0.CO;2 Download citation file: Ris (Zotero) Refmanager EasyBib Bookends Mendeley Papers EndNote RefWorks BibTex toolbar search Search Dropdown Menu toolbar search search input Search input auto suggest filter your search All ContentBy SocietyGSA Bulletin Search Advanced Search Abstract Along the International Program of Ocean Drilling (IPOD) Japan Trench transect, a mid-Cenozoic period of tectonism without arc volcanism separated an earlier Cretaceous to Paleogene and a later Neogene period of plate convergence and subduction. The Cretaceous to early Paleogene period of convergence is evidenced by andesitic volcanism associated with a large syncline, probably a forearc basin. The seaward flank of the basin is a tectonically thickened sediment sequence inferred to be an accretionary complex. The arc, the syncline, and the thickened sediment sequence resemble an arc-trench system of the size and structure of the Great Valley forearc basin and Franciscan accretionary complex of California, and they were probably continuations of the Yezo geosyncline and associated sequences exposed to the north on Hokkaido. The arc-trench system is contemporaneous with the adjacent Shimanto arc-trench system southwest of Tokyo Bay. In the early Paleogene, volcanism ceased, and part of the thickened sediment sequence of the Cretaceous-Paleogene margin was emergent as a 160-km-wide landmass which is recognized in seismic records as a later Paleogene sediment source. At the end of the Paleogene, this landmass began to subside and volcanism began again, but it was located first briefly on the east, and then on the west of the Cretaceous arc along the present arc of northern Honshu. The land-mass erosion surface is clearly visible as an angular unconformity in multichannel seismic-reflection records; the sequence of Neogene sediment, explosive volcanism, and benthic foraminiferal assemblages recording subsidence from subareal conditions to the present bathyal depths have been studied in Deep Sea Drilling Project (DSDP) cores. Cretaceous subduction appears to have resulted in a very extensive accretionary complex, whereas the Neogene subduction period appears to have been marked by little net accretion in the forearc area but massive subsidence and some erosion of the front of the convergent margin. This content is PDF only. Please click on the PDF icon to access. First Page Preview Close Modal You do not have access to this content, please speak to your institutional administrator if you feel you should have access.

The first deep borehole determinations of temperature gradients and heat flow on the landward wall of the Japan Trench and forearc were made on IPOD DSDP leg 57. These heat flow values are based on temperature logs corrected to equilibrium, using a detailed model of the drilling disturbance. Heat flow values on a deeply submerged marine terrace, landward of the trench slope break are 28 and 32 mW m−2. A measurement in the midslope terrace basin on the landward wall of the trench yielded a value of 22 mW m−2. The results are in good agreement with earlier seafloor measurements and indicate that most of the forearc area is characterized by heat flow about one half of that over oceanic lithosphere seaward of the trench. Our observations indicate only a small increase of heat flow from the trench to the volcanic arc, in agreement with thermal models, which suggests that the subduction of the relatively cold oceanic plate continues to dominate the temperature structure for distances of up to 250 km landward of the trench. The temperature profile in the borehole on the midslope terrace indicates possible vertical flow of pore waters. Hundreds of conductivity determinations were made using a new technique.

A detailed geothermal survey has been made on the western flank of the Mid‐Atlantic Ridge in the Brazil Basin where the crust is 20 m.y. old. The area is generally covered by a 150‐ to 200‐m thick layer of foraminiferal ooze, but basement outcrops are numerous. Sedimentary temperature profiles indicate anomalously low temperatures at the base of the sedimentary layer, which results from cold bottom water penetrating laterally into the upper igneous crust and absorbing much of the geothermal heat. Net influx rates of 10−8 m s−1 are implied by a simple aquifer model. A negative pressure drop across the sedimentary layer is required by this interpretation. Refraction studies indicate low seismic velocities (3.3 to 4.5 km s−1) near the top of layer 2, and a large velocity gradient with depth. The velocity structure in the upper kilometer of the crust is related to the porosity, from which it is inferred that permeabilities there are high. Many of the 52 temperature profiles show a significant decrease in gradient with depth. The curvature can be attributed to one or a combination of the following causes: (1) upward advection of pore water at rates of 10−7 s−1, (2) bottom water temperature variations, (3) variation of conductivity with depth, and (4) experimental errors. Interpretation of curvature in terms of an advective model leads to results hard to reconcile with present knowledge of pressure variations and permeabilities of the oceanic crust.

The study of oceanic crust continues to be important because of the presence of economic resources in oceanic areas and because many fundamental problems of geologic evolution are best solved from studies of the ocean. Although modeling and syntheses of existing data remain important, key breakthroughs in the future will come from the application of new technology such as multichannel towed seismic arrays, deep-towed side scan sonars, improved thermal probes, deep drilling, and satellite altimeters.

Journal of Geophysical Research: Solid EarthVolume 86, Issue B2 p. 1104-1104 CorrectionsFree Access Correction [to “Heat flow in the Bering Sea”] Marcus G. Langseth, Marcus G. LangsethSearch for more papers by this authorMichael A. Hobart, Michael A. HobartSearch for more papers by this authorKi-iti Horai, Ki-iti HoraiSearch for more papers by this author Marcus G. Langseth, Marcus G. LangsethSearch for more papers by this authorMichael A. Hobart, Michael A. HobartSearch for more papers by this authorKi-iti Horai, Ki-iti HoraiSearch for more papers by this author First published: 10 February 1981 https://doi.org/10.1029/JB086iB02p01104Citations: 1AboutPDF ToolsRequest permissionExport citationAdd to favoritesTrack citation ShareShare Give accessShare full text accessShare full-text accessPlease review our Terms and Conditions of Use and check box below to share full-text version of article.I have read and accept the Wiley Online Library Terms and Conditions of UseShareable LinkUse the link below to share a full-text version of this article with your friends and colleagues. Learn more.Copy URL No abstract is available for this article.Citing Literature Volume86, IssueB210 February 1981Pages 1104-1104 RelatedInformation

Coupling of the global heat flow, crustal heat source enrichment, thermal conductivity, and temperature in the crust and upper mantle of the moon is examined. A steady-state moon in which conductive heat transfer dominates is assumed. Heat-flow measurements from the Apollo 15 and 17 missions and gamma-ray mapping of thorium conducted by the Apollo 15 and 16 missions provide data for the study of the lunar thermal regime. Temperatures in the range of 1100 to 1600 K are found for the 300-km depth level. In the upper mantle, temperature gradients are in the range of 1.8 to 3.2 K/km.

Journal of Geophysical Research (1896-1977)Volume 82, Issue 23 p. 3391-3409 The mechanisms of heat transfer through the floor of the Indian Ocean Roger N. Anderson, Roger N. AndersonSearch for more papers by this authorMarcus G. Langseth, Marcus G. LangsethSearch for more papers by this authorJohn G. Sclater, John G. SclaterSearch for more papers by this author Roger N. Anderson, Roger N. AndersonSearch for more papers by this authorMarcus G. Langseth, Marcus G. LangsethSearch for more papers by this authorJohn G. Sclater, John G. SclaterSearch for more papers by this author First published: 10 August 1977 https://doi.org/10.1029/JB082i023p03391Citations: 217AboutPDF ToolsRequest permissionExport citationAdd to favoritesTrack citation ShareShare Give accessShare full text accessShare full-text accessPlease review our Terms and Conditions of Use and check box below to share full-text version of article.I have read and accept the Wiley Online Library Terms and Conditions of UseShareable LinkUse the link below to share a full-text version of this article with your friends and colleagues. Learn more.Copy URL Share a linkShare onEmailFacebookTwitterLinkedInRedditWechat Abstract We present 206 new heat flow measurements in the Indian Ocean. These and approximately 300 previously published heat flow values are individually evaluated for sedimentary environment and instrumental performance. The relationship between average heat flow and age is found to be little affected by selection of the most reliable experiments, although the scatter about the mean is significantly lowered. The variation of mean heat flow with age is found to be very similar to that in the eastern Pacific and Atlantic oceans: There is a crestal low heat flow zone with large variability, a transition zone within which the heat flow increases from values considerably below to values in agreement with predictions from thermal models of the oceanic lithosphere, and a region where heat flow values are in accord with theoretical predictions. However, the transition zone occurs over different crustal ages from ocean to ocean: 40–60 m.y. in the Indian Ocean, 4–6 m.y. in the Galápagos spreading center, 10–15 m.y. on the East Pacific Rise, and 50–70 m.y. on the Mid-Atlantic Ridge. The transition zone generally corresponds to a sea floor age where (1) sedimentary thickness increases to ≥300 m, (2) sea floor roughness is significantly smoothed by sediment blanketing, and (3) the carbonate content of surface sediments decreases to ≤40%. The transition zone occurs where water circulation in the oceanic crust stops affecting the surface heat flow strongly. There are two possible explanations for the transition. First, a change in composition from carbonate to siliceous sediments results in a decrease in bulk permeability. This combined with general thickening of the sedimentary blanket with aging results in the deposition of an impermeable layer which prevents the convective exchange of heat from the oceanic crust to the ocean. Second, hydrothermal flow within the oceanic crust is plugged by filling of circulation cracks in the oceanic crust. The fact that in several basins of the Indian Ocean the heat flow transition corresponds with the carbonatesiliceous boundary is support for the former mechanism. However, the fact that locations of increases in velocity of seismic layer 2A generally correspond to the transition regions in the Atlantic and Pacific oceans provides support for the latter mechanism. Heat flow measurements in the world's oceans allow us to calculate the variations of bulk permeability and basal temperature in the oceanic crust as a function of age and to evaluate the geochemical implications of the variation in these parameters between oceans. The combination of conductive heat flow and elevation versus age observations in old lithosphere demonstrates the deviation from t1/2 cooling in the Indian Ocean and indicates that the Mozambique and western Somali basins are considerably older than preliminary deep-sea drilling results suggest. 1 Supplementary table is available with entire article on microfiche. Order from American Geophysical Union, Suite 1000, 1909 K Street, N.W., Washington, D.C. 20006. Document J77-003; $1.00. Payment must accompany order. References Anderson, R. N., Petrological significance of low heat flow on the flanks of slow-spreading midocean ridges, Geol. Soc. Amer. Bull., 83, 2947–2956, 1972. Anderson, R. N., M. A. Hobart, The relation between heat flow, sediment thickness, and age in the eastern Pacific, J. Geophys. Res., 81, 2968–2989, 1976. Bodvarsson, G., R. P. Lowell, Ocean floor heat flow and the circulation of interstitial waters, J. Geophys. Res., 77, 4472–4475, 1972. Bookman, C. A., I. Malone, M. G. Langseth Jr., Sea floor geothermal measurements from Conrad cruise 13Tech. Reps. 5-CU-72, 1-CU-1-72, 279Columbia Univ., New York, 1972. Bryant, W. R., A. P. Deflache, P. K. Trabant, Consolidation of marine clays and carbonates, Deep Sea Sediments: Physical and Mechanical Properties A. L. Interlutzen, Plenum, New York, 1974. Corry, C., C. Dubois, V. Vacquier, Instrument for measuring terrestrial heat flow through the ocean floor, J. Mar. Res., 26, 165, 1968. Davis, E. E., C. R. B. Lister, Fundamentals of ridge crest topography, Earth Planet. Sci. Lett., 21, 405–413, 1974. Dorsey, N. E., Properties of Ordinary Water Substance, Hafner, New York, 1968. Elder, J. W., Physical processes in geothermal areas, Terrestrial Heat Flow Geophys. Monogr. Ser., 8 W. H. K. Lee, 211–239, AGU, Washington, D. C., 1965. Elder, J. W., Steady free convection in a porous medium heated from below, J. Fluid Mech., 27, 27–48, 1967. Forsyth, D. W., The evolution of the upper mantle beneath midocean ridges, J. Geophys. Res., 1977. Fox, P. J., S. E. DeLong, Healing of oceanic layer 2A: Geophysical and geological consequences (abstract), Eos Trans. AGU, 57, 329, 1976. Fox, P. J., E. Schreiber, J. J. Peterson, The geology of the oceanic crust: Compressional wave velocities of oceanic rocks, J. Geophys. Res., 78, 5155–5172, 1973. Gerard, R., M. Langseth, M. Ewing, Thermal gradient measurements in the water and bottom sediment of the western Atlantic, J. Geophys. Res., 67, 785–803, 1962. Helgeson, H. C., D. H. Kirkham, Theoretical prediction of the thermodynamic behavior of aqueous electrolytes at high pressures and temperatures, 1, Summary of the thermodynamic/electrostatic properties of the solvent, Amer. J. Sci., 274, 1089–1198, 1974. Herman, B. M., M. G. Langseth, M. A. Hobart, Heat flow in the oceanic crust bounding west Africa, Tectonophysics, 1977. Houtz, R., J. Ewing, Upper crustal structure as a function of plate age, J. Geophys. Res., 81, 2490–2498, 1976. Houtz, R. E., D. E. Hayes, R. G. Markl, Kerguelen Plateau: Bathymetric sediment distribution and crustal structure, Geol. Soc. Amer. Mem., 1977. Hyndman, R. D., D. S. Rankin, The Mid-Atlantic Ridge near 45°N, 18, Heat flow measurements, Can. J. Earth Sci., 9, 664–670, 1972. Hyndman, R. D., A. J. Erickson, R. P. Von Herzen, Geothermal measurements on DSDP leg 26, Initial Reports of the Deep-Sea Drilling Project, 26, 451–462, U.S. Government Printing Office, Washington, D. C., 1974. Hyndman, R. D., R. P. Von Herzen, A. J. Erickson, J. Jolivet, Heat flow measurements in deep crustal holes on the Mid-Atlantic Ridge, J. Geophys. Res., 81, 4053–4060, 1976. , Initial Reports of the Deep-Sea Drilling Project,, 22–26,U.S. Government Printing Office,Washington, D. C.,1974–1975. Kassoy, D. R., A. Zebib, Variable viscosity effects on the onset of convection in porous media, Phys. Fluids, 18, 1649–1651, 1975. Kolla, V., A. W. H. Be, P. Biscaye, Calcium carbonate distribution in the surface sediments of the Indian Ocean, J. Geophys. Res., 81, 2605–2616, 1976. Langseth, M. G., P. T. Taylor, Heat flow in the Indian Ocean, J. Geophys. Res., 72, 6249–6260, 1967. Langseth, M. G., R. P. Von Herzen, Heat flow through the floor of the world oceans, The Sea, 4 A. E. Maxwell, 299–352, Interscience, New York, 1970. Larson, R., Early Cretaceous breakup of Gondwanaland off western Australia, Geology, 5, 57–60, 1977. Lister, C. R. B., Heat flow west of the Juan de Fuca Ridge, J. Geophys. Res., 75, 2648–2654, 1970. Lister, C. R. B., On the thermal balance of a midocean ridge, Geophys. J. Roy. Astron. Soc., 26, 515–535, 1972. Lister, C. R. B., On the thermal balance of a midocean ridge, Geophys. J. Roy. Astron. Soc., 39, 465–509, 1974. Lowell, R. P., Circulation in fractures, hot springs, and convective heat transport on midocean ridge crests, Geophys. J. Roy. Astron. Soc., 40, 351–365, 1975. Markl, R. G., Evidence for the breakup of eastern Gondwanaland by the Early Cretaceous, Nature, 251, 196–200, 1974. Marshall, B. V., A. J. Erickson, Heat flow and thermal conductivity measurements, leg 25, Initial Reports of the Deep-Sea Drilling Project, 25, 349–355, U.S. Government Printing Office, Washington, D. C., 1975. McKenzie, D. P., Some remarks on heat flow and gravity anomalies, J. Geophys. Res., 72, 6261–6273, 1967. McKenzie, D. P., J. G. Sclater, The evolution of the Indian Ocean since the Late Cretaceous, Geophys. J. Roy. Astron. Soc., 25, 437–528, 1971. , National Academy of Sciences of the USSR, Geological-Geophysical Atlas of the Indian Ocean, Moscow, 1975. Parker, R. L., D. W. Oldenburg, A thermal model of oceanic ridges, Nature, 242, 137–139, 1973. Parsons, B., J. G. Sclater, An analysis of the variation of ocean floor heat flow and bathymetry with age, J. Geophys. Res., 82, 803–827, 1977. Popova, A. R., Ya. B. Smirnov, E. I. Suvilov, G. B. Udintsev, B. V. Shekhvatov, Geothermal studies on the largest tectonic structure of the bottom of the Indian Ocean, Investigations on the Problem Rift Zones of the World Oceans, 2, National Academy of Sciences of the USSR, Moscow, 1972. Ribando, R. J., K. E. Torrance, D. L. Turcotte, Numerical models for hydrothermal circulation in the oceanic crust, J. Geophys, Res., 81, 3007–3012, 1976. Richter, F. M., Convection and large-scale circulation of the mantle, J. Geophys. Res., 78, 8735–8745, 1973. Robertson, E. C., D. L. Peck, Thermal conductivity of vesicular basalt from Hawaii, J. Geophys. Res., 79, 4875–4888, 1974. Schlich, R., Sea floor spreading history and deep-sea drilling results in the Madagascar and Mascarene basins, western Indian Ocean, leg 26, Initial Reports of the Deep-Sea Drilling Project, 26, 663–678, U.S. Government Printing Office, Washington, D. C., 1974. Schlich, R., E. S. W. Simpson, T. L. Vallier, Regional aspects of DSDP in western Indian Ocean, leg 25, Initial Reports of the Deep-Sea Drilling Project, 25, 743–759, U.S. Government Printing Office, Washington, D. C., 1975. Schubert, G., C. Froidevaux, D. A. Yuen, Oceanic lithosphere and asthenosphere: Thermal and mechanical structure, J. Geophys. Res., 81, 3525–3540, 1976. Sclater, J. G., Heat flow in the northwest Indian Ocean and Red Sea, Phil. Trans. Roy. Soc. London, Ser. A, 259, 271–278, 1966. Sclater, J. G., R. L. Fisher, Evolution of the east central Indian Ocean with emphasis on the tectonic setting of the Ninety East Ridge, Geol. Soc. Amer. Bull., 85, 613–702, 1974. Sclater, J. G., J. Francheteau, The implications of terrestrial heat flow observations on current tectonic and geochemical models of the crust and upper mantle of the earth, Geophys. J. Roy. Astron. Soc., 20, 509–542, 1970. Sclater, J. G., K. D. Klitgord, A detailed heat flow, topographic, and magnetic survey across the Galápagos spreading center at 86oW, J. Geophys. Res., 78, 6951–6975, 1973. Sclater, J. G., R. N. Anderson, M. L. Bell, Elevation of ridges and evolution of the central eastern Pacific, J. Geophys. Res., 76, 7888–7915, 1971. Sclater, J. G., R. P. Von Herzen, D. L. Williams, R. N. Anderson, K. D. Klitgord, The heat flow low on the flank of the Galapagos spreading center, Geophys. J. Roy. Astron. Soc., 38, 609–626, 1974. Sclater, J. G., J. Crowe, R. N. Anderson, On the reliability of oceanic heat averages, J. Geophys. Res., 81, 2997–3006, 1976a. Sclater, J. G., B. P. Luyendyk, L. Meinke, Magnetic lineations in the southern part of the Central Indian Basin, Geol. Soc. Amer. Bull., 87, 371–378, 1976b. Shor, G. G., H. W. Menard, R. W. Raitt, Structure of the Pacific Basin, The Sea, 4 A. E. Maxwell, 3–28, Interscience, New York, 1970. Silverston, P. L., Warmedurchgang in waagerechten Flüssigkeitsschichten, 1, Forsch. Ingenieurw., 24, 29–3251–69, 1958. Skilbeck, J. N., R. N. Anderson, Heat flow and a two-layer model for convection in porous media: The oceanic crust and overlying sediments, J. Geophys. Res., 1977. Talwani, M., C. C. Windisch, M. G. Langseth, Reykjanes Ridge crest: A detailed geophysical study, J. Geophys. Res., 76, 473–517, 1971. Vacquier, V., P. T. Taylor, Geothermal and magnetic survey off the coast of Sumatra, Bull. Earthquake Res. Inst. Tokyo Univ., 44, 531–540, 1966. Von Herzen, R. P., Geothermal heat flow in the gulfs of California and Aden, Science, 140, 1207–1208, 1963. Von Herzen, R. P., M. G. Langseth, Present status of oceanic heat-flow measurements, Phys. Chem. Earth, 6, 365–407, 1966. Von Herzen, R. P., A. E. Maxwell, The measurement of thermal conductivity of deep-sea sediments by a needle probe method, J. Geophys. Res., 64, 1557–1563, 1959. Von Herzen, R. P., S. Uyeda, Heat flow through the eastern Pacific Ocean floor, J. Geophys. Res., 68, 4219–4250, 1963. Von Herzen, R. P., V. Vacquier, Heat flow and magnetic profiles on the Mid-Indian Ocean Ridge, Phil. Trans. Roy. Soc. London, Ser. A., 259, 262–270, 1966. Williams, D. L., R. P. Von Herzen, Heat loss from the earth: New estimate, Geology, 2, 327–328, 1974. Williams, D. L., R. P. Von Herzen, J. G. Sclater, R. N. Anderson, the Galapagos spreading center: Lithospheric cooling and hydrothermal circulation, Geophys. J. Roy. Astron. Soc., 38, 587–608, 1974. Citing Literature Volume82, Issue23Solid Earth and Planets10 August 1977Pages 3391-3409 ReferencesRelatedInformation