Sound velocity as a function of depth in marine sediments
Additional data from sonobuoys and the Deep Sea Drilling Project (DSDP) justify separating sound‐velocity‐depth functions and velocity gradients (in the first layer of soft marine sediments) into some geographic areas and sediment types. Based on sonobuoy and core measurements (where V is sound velo...
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American Institute of Physics
1985
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Online Access: | https://oceanrep.geomar.de/id/eprint/40037/ https://oceanrep.geomar.de/id/eprint/40037/1/Hamilton.pdf https://doi.org/10.1121/1.392905 |
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ftoceanrep:oai:oceanrep.geomar.de:40037 2023-05-15T15:43:49+02:00 Sound velocity as a function of depth in marine sediments Hamilton, Edwin L. 1985 text https://oceanrep.geomar.de/id/eprint/40037/ https://oceanrep.geomar.de/id/eprint/40037/1/Hamilton.pdf https://doi.org/10.1121/1.392905 en eng American Institute of Physics https://oceanrep.geomar.de/id/eprint/40037/1/Hamilton.pdf Hamilton, E. L. (1985) Sound velocity as a function of depth in marine sediments. Journal of the Acoustical Society of America, 78 (4). pp. 1348-1355. DOI 10.1121/1.392905 <https://doi.org/10.1121/1.392905>. doi:10.1121/1.392905 info:eu-repo/semantics/restrictedAccess Article PeerReviewed 1985 ftoceanrep https://doi.org/10.1121/1.392905 2023-04-07T15:36:07Z Additional data from sonobuoys and the Deep Sea Drilling Project (DSDP) justify separating sound‐velocity‐depth functions and velocity gradients (in the first layer of soft marine sediments) into some geographic areas and sediment types. Based on sonobuoy and core measurements (where V is sound velocity in km/s, and h is depth in sediments in km), the following data are obtained: continental shelf basins off Sumatra and Java—V=1.484+0.710h−0.085h2; U. S. Atlantic continental rise—V=1.513+0.828h−0.138h2; deep‐sea terrigenous sediments—V=1.519+1.227h−0.473h2; and siliceous sediments of the Bering Sea— V=1.509+0.869h−0.267h2. Selected DSDP data (through leg 74) in similar areas yield: continental terrace silt–clays—V=1.505+0.712h; deep‐sea terrigenous sediments—V=1.510+1.019h; and deep‐sea siliceous sediments—V=1.533+0.761h. Computed velocity gradients from sonobuoy measurements are generally supported by the DSDP gradients. Only DSDP data give the following: hemipelagic sediments—V=1.501+1.151h; deep‐sea calcareous sediments—V=1.541+0.928h; and deep‐sea pelagic clay—V=1.526+1.046h. Where fast sediment accumulation occurs, there has not been enough time to reduce sediment pore spaces under overburden pressure; areas of slow accumulation may have relatively high sediment structural strength. Both cases have lower velocity gradients because higher porosities and consequent lower velocities persist to deeper depths. Article in Journal/Newspaper Bering Sea OceanRep (GEOMAR Helmholtz Centre für Ocean Research Kiel) Bering Sea The Journal of the Acoustical Society of America 78 4 1348 1355 |
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Open Polar |
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OceanRep (GEOMAR Helmholtz Centre für Ocean Research Kiel) |
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ftoceanrep |
language |
English |
description |
Additional data from sonobuoys and the Deep Sea Drilling Project (DSDP) justify separating sound‐velocity‐depth functions and velocity gradients (in the first layer of soft marine sediments) into some geographic areas and sediment types. Based on sonobuoy and core measurements (where V is sound velocity in km/s, and h is depth in sediments in km), the following data are obtained: continental shelf basins off Sumatra and Java—V=1.484+0.710h−0.085h2; U. S. Atlantic continental rise—V=1.513+0.828h−0.138h2; deep‐sea terrigenous sediments—V=1.519+1.227h−0.473h2; and siliceous sediments of the Bering Sea— V=1.509+0.869h−0.267h2. Selected DSDP data (through leg 74) in similar areas yield: continental terrace silt–clays—V=1.505+0.712h; deep‐sea terrigenous sediments—V=1.510+1.019h; and deep‐sea siliceous sediments—V=1.533+0.761h. Computed velocity gradients from sonobuoy measurements are generally supported by the DSDP gradients. Only DSDP data give the following: hemipelagic sediments—V=1.501+1.151h; deep‐sea calcareous sediments—V=1.541+0.928h; and deep‐sea pelagic clay—V=1.526+1.046h. Where fast sediment accumulation occurs, there has not been enough time to reduce sediment pore spaces under overburden pressure; areas of slow accumulation may have relatively high sediment structural strength. Both cases have lower velocity gradients because higher porosities and consequent lower velocities persist to deeper depths. |
format |
Article in Journal/Newspaper |
author |
Hamilton, Edwin L. |
spellingShingle |
Hamilton, Edwin L. Sound velocity as a function of depth in marine sediments |
author_facet |
Hamilton, Edwin L. |
author_sort |
Hamilton, Edwin L. |
title |
Sound velocity as a function of depth in marine sediments |
title_short |
Sound velocity as a function of depth in marine sediments |
title_full |
Sound velocity as a function of depth in marine sediments |
title_fullStr |
Sound velocity as a function of depth in marine sediments |
title_full_unstemmed |
Sound velocity as a function of depth in marine sediments |
title_sort |
sound velocity as a function of depth in marine sediments |
publisher |
American Institute of Physics |
publishDate |
1985 |
url |
https://oceanrep.geomar.de/id/eprint/40037/ https://oceanrep.geomar.de/id/eprint/40037/1/Hamilton.pdf https://doi.org/10.1121/1.392905 |
geographic |
Bering Sea |
geographic_facet |
Bering Sea |
genre |
Bering Sea |
genre_facet |
Bering Sea |
op_relation |
https://oceanrep.geomar.de/id/eprint/40037/1/Hamilton.pdf Hamilton, E. L. (1985) Sound velocity as a function of depth in marine sediments. Journal of the Acoustical Society of America, 78 (4). pp. 1348-1355. DOI 10.1121/1.392905 <https://doi.org/10.1121/1.392905>. doi:10.1121/1.392905 |
op_rights |
info:eu-repo/semantics/restrictedAccess |
op_doi |
https://doi.org/10.1121/1.392905 |
container_title |
The Journal of the Acoustical Society of America |
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78 |
container_issue |
4 |
container_start_page |
1348 |
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1355 |
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