By J. L. Best, C. S. Bristow (editors)
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Extra info for Braided Rivers (Geological Society Special Publication 75)
However, the exponents in this type of relationship are not likely to apply to gravel-bed streams, and there is much overlap in stream power per unit bed area for natural meandering and braided rivers (Carson 1984b,c; Ferguson 1987). g. Straub 1935; Abdullayev 1973; Ashworth & Ferguson 1986; Bridge & Gabel 1992; Ferguson et al. 1992; Ashworth et al. g. g. Best 1986, 1987, 1988; Roy & Bergeron 1990; Roy & De Serres 1989; Ashmore et al. g. Bridge 1992). Channel geometry associated with multiplerow alternate bars at constant discharge is illustrated in Fig.
Bridge et al. 1986). Also, the relative sinuosities of channels on either side of braid bars is commonly such as to give a braid length/ maximum width of approximately 3-4, which. represents a streamlined form according tG Komar (1983, 1984). In many natural rivers, the riffle-riffle spacing, and overall bar dimensions do not change appreciably as discharge falls seasonally below 'channel-forming' discharge. However, if a braided channel segment experiences a reduction in discharge over a long enough term (relative to erosion and deposition rate), a series of bars and bends may develop that have a shorter wavelength than the original segment.
As the confluence angle increases the scour zone changes from trough shaped to more basin-like (Ashmore & Parker 1983; Best 1986). If the discharge of the entering channels are similar, the long axis of the scour tends to bisect the confluence angle (Best 1986). If one channel is dominant the scour zone tends to parallel the direction of this channel (Ashmore & Parker 1983; Best 1987; Figs 7 and 9). The maximum depth of scour (ds) is commonly expressed as a function of the average depth of the joining channels (dl, d2) at channel- 34 J .
Braided Rivers (Geological Society Special Publication 75) by J. L. Best, C. S. Bristow (editors)