1 Oc679 Acoustical Oceanography Sound scattered by a body (Medwin & Clay Ch 7) scattering is the consequence of the combined processes of reflection, refraction and diffraction at surfaces marked by inhomogeneities in , c - these may be external or internal to a scattering volume ( internal inhomogeneities important when considering scattering from fish, for example ) net result of scattering is a redistribution of sound pressure in space – changes in both direction and amplitude for a monostatic system, we are most interested in the sound reflected back to the source/receiver – this is termed backscatter scattering is wavelength- (frequency, sort of) dependent the sum total of scattering contributions from all scatterers is termed reverberation this is heard as a long, slowly decaying quivering tonal blast following the ping of an active sonar system to start, we consider simple, hard, individual scatterers

2 Oc679 Acoustical Oceanography reverb following explosive charge initial surface reverb is sharp, followed by tail due to multiple reflection & scattering then volume reverb in mid-water column (incl. deep scattering layer) then bottom reflection, 2 nd surface reflection, and long tail of bottom reverb explosive source at 250 m nearby receiver at 40 m bottom depth 2000 m

3 Oc679 Acoustical Oceanography transmission is a gated sinusoid or ping of duration t p sound pressure scattered by a small object – crests of sinusoid indicated as a sequence of wave fronts in this sketch ,  dependencies of incident wave are suppressed (this would be due to source beam pattern) for simplicity wavefronts drawn as if coming from center of object – for a complex object, as shown, there would be many interfering wave fronts spreading from the object within shadow, interference of incident and scattered waves is destructive as incident and scattered waves arrive at the same time with same amplitude, but out-of-phase outside of shadow, interference of incident and scattered waves forms a penumbra (partial shadow) beyond penumbra (  <  interfer ), incident and scattered waves can be separated (no interference)

4 Oc679 Acoustical Oceanography traces of incident and scattered sound pressures – ping has duration t p travel time for sound to scatter to receiver is R/c (here R is measured from the scattering object) this is referred to previous figure = 0, otherwise, incident sound pressure:scattered sound pressure: Complex Acoustical Scattering Length, consider amplitude and ignore phase or dimension is length, unrelated to any length scale of the body = 0, otherwise, p scat (t) = P scat e i2πf(t-R/c)

5 Oc679 Acoustical Oceanography Differential Scattering Cross-section, dimension area [ m 2 ] here,  s, L, and P scat all depend on the geometry of the measurement and the carrier frequency, f, of the ping (really they depend on wavelength) above is a bistatic representation in which source and receiver are at different positions when at same position (monostatic), it is called backscatter now  = 0 and  = 0, and differential backscattering cross-section

6 Oc679 Acoustical Oceanography total scattering cross section total scattering cross-section is the integral of over total solid angle  scat is the total power scattered by the body note that so far we have only considered the differential (and have used  ) – that is we have only considered a differential portion of the total radiated power from the scattering body – this is done by looking at only a portion of the 3D surface with a finite receiver such as shown in the schematic sketch or

7 Oc679 Acoustical Oceanography target strength logarithmic measure of differential cross-section reference area is 1 m 2 for backscatter relative to scattering length or backscattering length

8 Oc679 Acoustical Oceanography where P 0 is referred to R 0 (usually 1 m) travel time source to receiver is R/c sound spreads spherically from source and then from object single source/receiver, P scat e i2πft = P 0 e i2πf(t-R/c) R 0 L bs (f) 10 -2αR/20 /R 2 P inc e i2πft = P 0 e i2πf(t-R/c) R αR/20 /R how do we quantify a single transducer measurement – R now referenced to transducer location

9 Oc679 Acoustical Oceanography Scattering by spheres simple shape, well studied an acoustically small and compact non-spherical body scatters in about the same way as a sphere of same volume and same average physical characteristics ( , c) acoustically small  ( ka << 1 ) dimensions much less than those of incident sound wavelength 1)rigid sphere ka >> 1reflection dominates, geometrical or specular scattering 2)rigid sphere ka << 1diffraction dominates, Rayleigh scattering 3)fluid sphere – includes transmission through medium

10 Oc679 Acoustical Oceanography geometrical scatter from a rigid sphere ( ka >> 1 ) specular (mirrorlike) reflection in the Kirchoff approximation ( discussed in text) plane waves reflect from an area as if the local, curved surface is a plane scatter consists of a spray of reflected waves each obeying simple reflection law – that is, angle of reflection = angle of incidence – we will employ a ray solution diffraction effects are ignored - these would come from edge of shadow and behind sphere we will calculate the scattering from a fixed, rigid, perfectly reflecting sphere at very high frequencies ( ka >> 1 ) incident sound is a plane wave of intensity I inc no energy absorption in medium no energy penetrates surface of sphere short wavelengths ka >> 1 or big objects

11 Oc679 Acoustical Oceanography a dSidSi adiadi ii 2asin  i dS i cos  i d  i is a ring increment about the sphere 1 st we need to know the incoming power at angle  i surface area increment (corresponding to grey shaded area) component in direction of incident wave input power to ring short wavelengths ka >> 1 or big objects

12 Oc679 Acoustical Oceanography now, calculate scattered power incident rays within angular increment d  i at angle  i are scattered within increment d  s =2d  i at angle  s =2  i the geometrically-scattered power measured at range R is assume all incident power is scattered [ no power loss ] then and in terms of scattering length [ we will get back to this later ] result: scattered intensity is independent of angle of incidence – which should be the case by symmetry of the sphere, but is not the case in general in the case of the sphere, this means that all differential geometrical scattering cross-sections, including backscattering cross-sections, are equal short wavelengths ka >> 1 or big objects

13 Oc679 Acoustical Oceanography the differential scattering cross-section is: and the total geometrical scattering cross-section is, where  a 2 is the cross-sectional area  gs does not include the effects of diffraction, so is not the total scattering cross-section the ray solution is deceptively simple: is accurate in the backscatter direction 0-90  but it ignores the complicated interference patterns beyond 90  more complete calculations using wave theory indicate that the total scattering cross-section approaches twice its geometrical cross-section (2  a 2 ) for large ka short wavelengths ka >> 1 >> short wavelengths ka >> 1 or big objects

14 Oc679 Acoustical Oceanography Rayleigh scatter from a sphere ka << 1 long wavelengths ka << 1 or small objects when the wavelength is large compared to the sphere radius, scatter is due solely to diffraction. 2 simple conditions cause scatter: 1.monopole radiation – in the case that the bulk elasticity (E 1 ) of the sphere (recall E = p  A /  = compressibility -1 ) is less than that of water (E 0 ), the incident condensations and rarefactions compress and expand the body, thereby reradiating a spherical wave – phase reversed if E 1 >E 0 2. dipole radiation – if the sphere’s density (  1 ) is much greater than that of the medium (  0 ), the body’s inertia will cause it to lag behind as the plane wave oscillates (sloshes back and forth). This motion is equivalent to the water being at rest and the body being in oscillation. This motion generates a dipole reradiation. When  1 <  0, the effect is the same but the phase is reversed. In general, when  1   0, the scattered pressure is proportional to cos , where  is the angle between scattered and incident directions.

15 Oc679 Acoustical Oceanography long wavelengths ka << 1 M&C develop a solution for the monopole and dipole radiation independently and then sum them the scattered pressure is: scattering length and cross-sections determined by referencing R to 1 m backscatter determined by setting  = 0 Rayleigh scattering geometrical scattering peaks, troughs at ka>1 due to interference between diffracted wave around periphery and wave reflected at front surface of sphere relative scattering cross-section is obtained by /  a 2 and is  (ka) 4 result: the acoustical scattering cross-section for Rayleigh scatter is much less than for geometrical scatter because sound waves bend around and are almost unaffected by acoustically small, non-resonant bodies long wavelengths ka << 1 or small objects

16 Oc679 Acoustical Oceanography fluid sphere, Rayleigh scattering ( ka << 1) more general case, when sphere is an elastic fluid g =  1 /  0, ratio of sphere’s density to medium density h = c 1 /c 0 e = E 1 /E 0  = angle between incident and scatter directions [ backscatter determined for  = 0  ] monopole component dipole component most bodies in the sea have values of e and g close to unity and both terms are of similar importance bubbles have e << 1 and g << 1 - in this case the monopole term dominates - highly compressible bodies such as bubbles are capable of resonating when ka << 1 - resonant bubbles produce scattering cross-sections several orders of magnitude greater than geometrical

17 small target compared to λ ka << 1 Rayleigh scattering large target compared to λ ka << 1 geometrical scattering

18 Oc679 Acoustical Oceanography scattering of light follows essentially the same scattering laws as sound but light wavelengths are much smaller than sound - O(100s of nm) almost all scattering bodies in seawater are large compared to optical wavelengths and have optical cross-sections equal to their geometrical cross-sections  the sea is turbid to light on the other hand, acoustic wavelengths are typically large compared to scattering bodies found in seawater (at 300 kHz,  5 mm, 4 orders of magnitude larger) - acoustic scattering is dominated by Rayleigh scattering by comparison the sea is transparent to sound - what limits the propagation of 300 kHz sound is not scattering but absorption

19 Oc679 Acoustical Oceanography why is the sky blue? Rayleigh scattering α 1/λ 4 λ blue << λ red reds pass through atmosphere without scattering but blues are scattered from O 2 molecules and enters our eyes from a range of angles violet scattered even better but our eyes are less sensitive to this sunrise/sunset at low azimuth, light passes through extended range of atmosphere blue completely scattered out and sun appears red green flash occurs at the very end of the sunset (beginning of sunrise, when sun has passed below horizon shorter wavelengths refracted more effectively than longer wavelengths blue has been scattered out, reds are not effectively refracted what’s left if green (sometimes very bright and pops up above horizon for < 1s)

20 scattering from microstructure hints of scattering from internal waves and microstructure in 60s, 70s but confusing because of bio-scattering alternatively, bio-scattering may be confused with microstructure scattering leading to errors in estimating plankton populations scattering cross-sections were computed based on Tatarski’s computations for atmospheric radar (Proni & Apel 1975) these were based on turbulence structure functions note: these included the effects of velocity fluctuations as well as T (or c) fluctuations but u air /c air >> u water /c water

21 1 st experimental evidence from controlled experiments in Wellington reservoir, W. Australia (Thorpe & Brubaker, 1983) “Observations of sound reflection by temperature microstructure” L&O Known sources Towed cylinder and weights at fixed depths from vessel 1 Measured using 102 kHz sounder from vessel 2 results 1.no signal when towed in mixed layer – thus velocity fluctuations do not contribute 2.clear signal of cylinder and weight wakes in stratified regions 3.estimates of energy dissipated by towed cylinder permitted estimates of turbulence quantities, to which scattering theory could be compared a-a, b-b, c-c are natural scatterers

22 theories employ the use of robust statistical models of turbulence spectra Batchelor, 1957 (“wave scattering due to turbulence” Proc.Symp.Nav.Hydro.) Goodman, 1990 (considers the bistatic or multistatic problem, not just backscatter) Ross etal 2004

23 Ross etal 2004

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High-frequency acoustics – this is an important tool to help detect instabilities that lead to turbulence scattering from small-scale sound speed fluctuations caused by T and S microstructure sound speed c=c(T,p) Ross and Lueck 2003

26 but here’s the problem

27 Andone Lavery WHOI Lavery etal 2009

28 Lavery etal 2009

29 Lavery etal 2009

30 Lavery etal 2009

31 Lavery etal 2010

32 here all scattering is bio. note difference in low k spectra which tend to decrease toward low k compared to turbulence spectra

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36 Oc679 Acoustical Oceanography coordinate systems rectangular cylindrical spherical

37 Oc679 Acoustical Oceanography an object is effectively insonified by plane waves when its dimensions are smaller than the 1 st Fresnel zone – within the 1 st Fresnel zone, a spherical wavefront can be approximated as a plane wave

38 Urick Oc679 Acoustical Oceanography definition of volume scattering strength (or backscattering strength if referred to same source and receiver in term of surface scattering can define a surface scattering strength note: the distinction in the definitions – the volume scattering strength S v is defined by the ratio I scat /I inc, each referenced to 1 m (or 1 yd) from the object in M&C terms (that we have so far), I scat is referenced to the receiver at range R from the object while I inc referred to 1 m from object– the inclusion of attenuation and spherical spreading (1/R 2 ) gives the length scale unit

39 Oc679 Acoustical Oceanography Urick fig 8.3 a more complete schematic of the problem includes beam pattern of single transducer as both source (b) and receiver (b’) ( here absorption ignored ) I 0 is the axial intensity at unit distance (source level SL = 10 logI 0 ) intensity at 1 m in direction ( ,  ) is I 0 b( ,  ) incident intensity at dV is I 0 b( ,  )/r 2 intensity backscattered at P 1 m back toward source is (I 0 b( ,  )/r 2 )S v dV scattered intensity at source is (I 0 b( ,  )/r 4 )S v dV, where it is assumed that sound spreads spherically from both source and object dV receiver will produce voltage (rms) R 2 (I 0 b( ,  )b’( ,  )/r 4 )S v dV where R is the receiver sensitivity total receiver output is  V[(R 2 I 0 SV /r 4 ) b( ,  )b’( ,  )] dV