Changes

===Bounding Surfaces That Define Rock Volume===

===Bounding Surfaces That Define Rock Volume===

Each set of shoreline clinoforms is contained within a distinct, upward-shallowing, regressive succession, or parasequence (sensu Van Wagoner et al., 1990; Hampson et al.,<ref name=Hmpsn2008 />), that is bounded at its base and top by flooding surfaces. Multiple clinoforms exist within each parasequence. Because the algorithm is generic, any top and base bounding surfaces can be used; the only requirement is that the top bounding surface is entirely above, or coincident with, the base bounding surface across the model volume ([[:File:BLTN13190fig1.jpg|Figure 1A–C]]). By using the flooding surfaces at the top and/or base of a parasequence as reference surfaces, the algorithm can produce clinoforms that are modified by postdepositional folding and faulting ([[:File:BLTN13190fig2.jpg|Figure 2A]]), truncation by overlying erosion surfaces ([[:File:BLTN13190fig2.jpg|Figure 2B]]), and/or progradation over irregular sea-floor topography ([[:File:BLTN13190fig2.jpg|Figure 2C]]). The parasequence-bounding flooding surfaces are first read into the clinoform-modeling algorithm, using a standard gridded format exported from a reservoir modeling software package. Clinoforms created by the algorithm adapt to the morphology of either (or both) bounding surfaces, using a height function, h(r_c) ([[:File:BLTN13190fig2.jpg|Figure 2D]]), that calculates the height of the clinoform relative to the length along the clinoform surface and the height difference between the top and base bounding surfaces (see Table 1 for nomenclature):  

Each set of shoreline clinoforms is contained within a distinct, upward-shallowing, regressive succession, or parasequence (sensu Van Wagoner et al.;<ref>Van Wagoner, J. C., R. M. Mitchum, K. M. Campion, and V. D. Rahmanian, 1990, Siliciclastic sequence stratigraphy in well logs, cores and outcrops: Concepts for high-resolution correlation of time and facies: [http://store.aapg.org/detail.aspx?id=1196 AAPG Methods in Exploration Series, no. 7], 55 p.</ref> Hampson et al.,<ref name=Hmpsn2008 />), that is bounded at its base and top by flooding surfaces. Multiple clinoforms exist within each parasequence. Because the algorithm is generic, any top and base bounding surfaces can be used; the only requirement is that the top bounding surface is entirely above, or coincident with, the base bounding surface across the model volume ([[:File:BLTN13190fig1.jpg|Figure 1A–C]]). By using the flooding surfaces at the top and/or base of a parasequence as reference surfaces, the algorithm can produce clinoforms that are modified by postdepositional folding and faulting ([[:File:BLTN13190fig2.jpg|Figure 2A]]), truncation by overlying erosion surfaces ([[:File:BLTN13190fig2.jpg|Figure 2B]]), and/or progradation over irregular sea-floor topography ([[:File:BLTN13190fig2.jpg|Figure 2C]]). The parasequence-bounding flooding surfaces are first read into the clinoform-modeling algorithm, using a standard gridded format exported from a reservoir modeling software package. Clinoforms created by the algorithm adapt to the morphology of either (or both) bounding surfaces, using a height function, h(r_c) ([[:File:BLTN13190fig2.jpg|Figure 2D]]), that calculates the height of the clinoform relative to the length along the clinoform surface and the height difference between the top and base bounding surfaces (see Table 1 for nomenclature):  

:<math>h(r_c) = (h_{\text{max}}(r_c) - h_{\text{min}}(r_c)) - \left[ \frac{(r_c(x, y) - r_{\text{min}}(x, y))}{(r_{\text{max}}(x, y) - r_{\text{min}}(x, y)} (h_{\text{max}}(r_c) - h_{\text{min}}(r_c)) \right ]</math>

:<math>h(r_c) = (h_{\text{max}}(r_c) - h_{\text{min}}(r_c)) - \left[ \frac{(r_c(x, y) - r_{\text{min}}(x, y))}{(r_{\text{max}}(x, y) - r_{\text{min}}(x, y)} (h_{\text{max}}(r_c) - h_{\text{min}}(r_c)) \right ]</math>

# Steckler, M. S., G. S. Mountain, K. G. Miller, and N. Christie-Blick, 1999, Reconstruction of tertiary progradation and clinoform development on the New Jersey passive margin by 2D backstripping: Marine Geology, v. 154, no. 1–4, p. 399–420, doi: 10.1016/S0025-3227(98)00126-1.

# Steckler, M. S., G. S. Mountain, K. G. Miller, and N. Christie-Blick, 1999, Reconstruction of tertiary progradation and clinoform development on the New Jersey passive margin by 2D backstripping: Marine Geology, v. 154, no. 1–4, p. 399–420, doi: 10.1016/S0025-3227(98)00126-1.

# Swift, D. J., 1968, Coastal erosion and transgressive stratigraphy: Journal of Geology, v. 76, no. 4, p. 444–456, doi: 10.1086/jg.1968.76.issue-4.

# Swift, D. J., 1968, Coastal erosion and transgressive stratigraphy: Journal of Geology, v. 76, no. 4, p. 444–456, doi: 10.1086/jg.1968.76.issue-4.

# Van Wagoner, J. C., R. M. Mitchum, K. M. Campion, and V. D. Rahmanian, 1990, Siliciclastic sequence stratigraphy in well logs, cores and outcrops: Concepts for high-resolution correlation of time and facies: AAPG Methods in Exploration Series, no. 7, 55 p.

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# Vinje, J., R. Nybø, and G. Grinestaff, 2011, A new simulation grid type is demonstrated for the giant Troll oil and gas field: SPE Paper 148023, 14 p.

# Vinje, J., R. Nybø, and G. Grinestaff, 2011, A new simulation grid type is demonstrated for the giant Troll oil and gas field: SPE Paper 148023, 14 p.

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