Changes

==Marine diagenesis==

==Marine diagenesis==

[[file:predicting-reservoir-system-quality-and-performance_fig9-52.png|300px|thumb|{{figure number|2}} Typical diagenetic pathways for marine sediments. Copyright: Burley et al.;<ref name=Burley1985>Burley, S. D., J. D. Kantorowicz, and B. Waugh, 1985, Clastic diagenesis, in P. J. Brenchley and B. P. J. Williams, eds., Sedimentology: Recent Developments and Applied Aspects: London, Blackwell Scientific Publications, p. 189–228.</ref> courtesy Blackwell Scientific.]]

[[file:predicting-reservoir-system-quality-and-performance_fig9-52.png|300px|thumb|{{figure number|2}} Typical diagenetic pathways for marine sediments. Copyright: Burley et al.;<ref name=ch09r7 /> courtesy Blackwell Scientific.]]

The precipitation of cements in quartzarenites and subarkoses deposited in a marine environment tends to follow a predictable pattern beginning with clay authigenesis associated with quartz and feldspar overgrowths, followed by carbonate precipitation. Clay minerals form first because they precipitate more easily than quartz and feldspar overgrowths, which require more ordered crystal growth. Carbonate cement stops the further diagenesis of aluminosilicate minerals.

The precipitation of cements in quartzarenites and subarkoses deposited in a marine environment tends to follow a predictable pattern beginning with clay authigenesis associated with quartz and feldspar overgrowths, followed by carbonate precipitation. Clay minerals form first because they precipitate more easily than quartz and feldspar overgrowths, which require more ordered crystal growth. Carbonate cement stops the further diagenesis of aluminosilicate minerals.