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<br /> 800 800 <br /> March 25 and 261 1967 May 5 and 6,1967 <br /> 700 700 <br />~ ~ <br /> 600 '" <br />'" 600 ... <br />... .___Flow 0 <br />0 ~ <br />~ <br />LIJ 500 500 LIJ <br /> (.!) <br />(.!) ~ 's--- 0:: <br />0:: <br /><t Salinity <t <br /> " 400 :J: <br />:J: 400 " , -- <br />() " -- ....- () <br />en Iq -'-0- en <br />0 300 I 0-' 300 0 <br /> r <br /> 1\ <br /> <br /> <br />Table 1. 1. <br /> <br />Salinity sources (taken from Mbbs <br />1970). <br /> <br />Contribution <br />from <br />Precipitation <br />(percent) <br /> <br />Contribution <br />from <br />Rocks <br />(percent) <br /> <br />l\;") <br />0..- <br />~ <br />c.o <br /> <br />Salinity <br />Sources <br /> <br />Rio Te fe (rain- <br />dominated river <br />type) <br /> <br />81 <br /> <br />19 <br /> <br />Ucayali (rock- <br />dominated river <br />type) <br /> <br />4,8 <br /> <br />95.2 <br /> <br />Rio Grande (evapora- <br />tion-crystallization <br />river type) <br /> <br />0,1 <br /> <br />99,9 <br /> <br />Bitter Creek Waterhsed, are shown by Figure <br />1.5. The authors obtained a correlation <br />coefficient (r2) of 0.53 when applying the <br />common exponential function, Equation 1.3, to <br />the runoff events. By utilizing monthly <br />average values and multivariate regression a <br />correlation coefficient (r2) of 0.8 was <br />a ch ieved. <br /> <br />Hsll (1970 snd 1971) derived six models <br />relating TDS to streamflow based upon the <br />equations: <br /> <br />dL = C dV + V dC <br />dt dt dt <br /> <br />(1. 12) <br /> <br /> <br />200 <br /> <br />o <br /> <br />4 e 12 16 20 0 <br />HOURS <br /> <br />d.\l <br />dt=Q-r <br />V = aQb <br /> <br /> <br />(1. 13) <br /> <br />(1.14) <br /> <br />in which <br /> <br />L = Total load <br />V = Volume <br />t Time <br />I = Inflow <br />a and b = Constants <br /> <br />His models describe steady-state syatems <br />Bnd do not account for hysteresis effects <br />accompanying rising and falling stages. The <br />equations are empirical, and the constants <br />sre best estimsted by statistical fit, <br /> <br />Lane (1975) described salt contribu- <br />tions for surface flows as originating <br />pr imsrily from dissolution of efflorescence <br />and mechanical weathering. Thus, the resul- <br />tant concentration might be described as a <br />function of both current and antecedent <br />flows, Thst is, if antecedent flows have <br />been high, then few salts would exist on the <br />soil surface. If the antecedent flows have <br />been low, then the availability of surfsce <br />salts probsbly would be high. He proposed <br />the general relationship illustrsted by <br />Figure 1.6. <br /> <br />Salinity models <br /> <br />Several deterministic snd psrametrlc <br />watershed salinity models have been developed <br />at Utsh State University. Hyatt et a1. <br /> <br />4 e 12 <br />HOURS <br /> <br />200 <br />16 20 <br /> <br />Figure 1. 5, <br /> <br />Flow (cfs) and salinity (ppm) for typical storms on the West Bitter Creek water- <br />shed. Oklahoma (taken from Pionke and Nicks 1970). <br /> <br />6 <br />