J. P. Riley and R. Chester (Eds.)'s Chemical Oceanography PDF

By J. P. Riley and R. Chester (Eds.)

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3 0 . 6 . , 1 9 7 0 ) . ment burial. In contrast, the I/C(org) ratios of surface sediments forming under reducing conditions show values one order of magnitude lower than those of oxidizing sediments, and during their burial the change in I/C(org) ratio is minimal (Price and Calvert, 1973). The differences in uptake of iodine by organic matter at the surface of oxidizing and reducing sediments, and its release or lack of release during burial, in all probability relates to differences in composition and behaviour of unspecified organic substances, formed by the degradation of organic matter, under different redox, and hence bacterial conditions.

Thus, in some respects the existence of siderite in marine sediments suffers many of the constraints of vivianite. However, within nonmarine environments, in which SO4" concentrations and hence those of H S " , are usually low, the only factors restricting the formation of these two minerals are changes in p H and the presence of competitive concentrations of elements such as calcium. Hence, both vivianite and siderite have been found in many nonmarine environments (see Rosenquist, 1970; James, 1966).

BRIAN PRICE retained within sediments (Hurd, 1972). Organic-rich sediments seem to retain more opal than do oxidising sediments. F o r instance, diatoms in organic rich anoxic sediments in saline lakes (pH = 9) on M o u n t Meru, Lahar, East Africa (Heckey, 1971) show little evidence of dissolution, even though the sediment interstitial water (pH = 8-5-9-0) contains very low _ 1 concentrations of S i 0 2 ( < 10 mg S i 0 2 l ) . The reason for this is probably the existence of an organic coating on the diatoms which inhibits dissolution.

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