By Darrell R. Jackson, Michael D. Richardson (auth.)

High-Frequency Seafloor Acoustics is the 1st booklet in a brand new sequence subsidized
by the place of work of Naval examine at the most recent learn in underwater acoustics.
This fascinating new name presents prepared entry to experimental information, concept, and
models suitable to high-frequency seafloor acoustics and should be of curiosity to
sonar engineers and researchers operating in underwater acoustics. The actual
characteristics of the seafloor affecting acoustic propagation and scattering are
covered, together with actual and geoacoustic homes and floor roughness.
Current theories for acoustic propagation in sediments are awarded alongside
with corresponding types for mirrored image, scattering, and seafloor penetration.
The major textual content is sponsored up by means of an intensive bibliography and technical appendices.

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The other advantage is that textural types can be determined from disturbed sediment samples, such as grab samples, whereas bulk properties such as density, permeability, and sound speed are altered by these collection methods. Methods to determine sediment grain size and other textural and bulk properties of sediment are discussed in Chs. 4 and 5. , water depth). Coarse sediments (gravel and sand), for example, tend to accumulate near shore, whereas fine sediments (silt and clay) tend to accumulate farther from shore.

1998a, Ransom et al. 2 Sediment Structure 39 Fig. 4. Fabric of recently settled organic-rich clay aggregates from Eckernf¨orde Bay, Baltic Sea (TEM image from [Anandarajah and Lavoie 2002]). Note the large void spaces, channels within and especially between clay aggregates, and abundant organic matter within channels (OM fc), as discrete blobs (OM b), and as biogenic remains. Bennett et al. 1999, Hulbert et al. 2002]. 11 g cm−3 ) (Fig. 4). The importance of organic matter in binding clay particles into larger aggregates may be greatly underestimated, and organic matter, in the form of long polymer strings, may be the dominant bonding mechanism in recently deposited sediments.

Kaolinite is a two-layer (1:1) or (T:O) clay mineral, whereas illite and smectite are three-layer clay minerals (2:1) or (2T:O), and chlorite is a four-layer clay mineral (2:1:1) or (2T:O:brucite). within layers. 05 to 2 μm, and kaolinite can occur in 3000 to 4000 sized stacks. 68 with a specific surface area of 10–20 m2 g−1 and a cation exchange capacity of 3–15 milliequivalent (mEq) per 100 g dry weight of clay. 66 )O20 (OH)4 ·nH2 O] is a three-layer (2:1) clay mineral that consists of an aluminum octahedral and magnesium and sodium tetrahedral sheets with weak interlayer bonding and isomorphic substitution by magnesium or other cations for aluminum in the octahedra and aluminum for silicon in the tetrahedra.

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