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Distributed Acoustic Sensing in Geophysics


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can be generalized for a nonzero length optical pulse e(z) directly from Equation 1.5 in the same way that an optical incoherent image was obtained in Goodman (2005) using correlation averaging 〈(ar1)(ar2)〉 = 〈a2〉 ⊗ 〈r1r2〉. This expression is valid for an uncorrelated field, generated by random reflection points 〈r1(z1)r2(z2)〉 = δ(z1z2). This calculation confirms that Equation 1.11 remains the same, as it represents averaging over different harmonic signals, but Equation 1.10 will be reshaped to:

image

      Phase measurements can be made in a more practical way than locking the interferometer onto a fringe by using intensity trace Ij(z, t) j = 1, 2, ..P from P multiple interferometers with different phase shifts. Such data can be collected consequentially in P optical pulses, but it reduces sensor bandwidth by P times. Alternatively, the information can be collected for one pulse using a multi‐output optical component, such as a 3×3 coupler. In the general case, the phase shift Φ(z, t) can be represented (Todd, 2011) via the arctangent function ATAN of the ratio of imaginary Im Z to real part Re Z of linear combinations of intensities:

      (1.16)upper V equals StartRoot Im upper Z squared plus Re upper Z squared EndRoot