Print this page
Click to view article in PDF format
Salt System Evolution of the Northern Paradox Basin*
Manuel Paz1, Bruce Trudgill2 and Chuck Kluth2
Search and Discovery Article #30078 (2009)
Posted March 20, 2009
*Adapted from extended abstract presented at AAPG Convention, San Antonio, TX, April 20-23, 2008
1Occidental Petroleum Corporation, Tupman, CA ( [email protected] )
2Colorado School of Mines, Golden, CO
The northern Paradox Basin in SE Utah and SW Colorado is characterized by a variety of salt-related structures ranging from deeply buried salt pillows to faulted diapirs and salt walls exposed at the surface (Figure 1 ).
By restoring a series of 2D structural cross sections, it was determined that the proximal Cutler Group (Permian) is a basinward prograding unit that caused underlying salt within the Paradox Formation Pennsylvanian) to flow in that same direction, towards the southwest (Figures 2, 3, 4, 5, 6 and 7 ). Under this scheme, more proximal salt structures evolved earlier than the more distal ones. During the early stages of progradation, there is a nondepositional hiatus in the distal part of the Paradox Basin. Salt withdrawal depended on the amount of mobile salt available and therefore facies within the Paradox Formation.
Depocenters on the east side of the Salt Valley salt wall migrated to the northwest during the early stages of the Cutler Group deposition, and then to the west (Figures 8 and 9). In that same area, welding out of the mobile salt occurred at the end of the Cutler time, although the present-day weld configuration was reached by Chinle time (Triassic).
The highest rates of sediment accumulation, salt wall growth, salt evacuation (in welded areas), salt area decrease and subsidence occurred during Cutler time, when the Uncompahgre Uplift was most active. Under the foreland basin framework, a wedge-top zone was interpreted close or on top of the Uncompahgre Uplift, where post-depositional deformation and cannibalization reincorporated the overlying sediments into the active depositional regime.
This understanding of the salt system evolution in the northern Paradox Basin impacts future oil exploration targets by defining a series of play concepts within the Paradox Formation, Honaker Trail Formation, Cutler Group, and White Rim Sandstone (Figure 10).
|
|
Relevant results of the present study include:
·
Based
on clinoforms observed in
· Under this scenario, the easternmost Onion Creek salt wall was the first structure to start growing, the Castle Valley salt wall was the second, and the Moab salt wall located to the west was the last one.
· By Honaker Trail time (Missourian-Virgilian) the salt system was already active, as indicated by thinning of this unit towards the Salt Valley salt wall. Deposition associated to salt mobilization was active until the end of Chinle time, indicating that the salt system was active during a period of ~100 m.y.
· During the early progradational stages (P1-P3), the distal part of the Paradox Basin was under erosion and/or nondeposition. So, in this part of the basin it is likely that a nondepositional hiatus between the Honaker Trail Formation and the overlying Cutler Group developed.
·
Mobilized
salt within the Paradox Formation is heterogeneous. To the east of the Onion
Creek salt wall,
· The P1 depocenter for the Salt Valley was the same as for the Onion Creek. By P2 time, there were separate depocenters for each salt wall, and after that the Salt Valley depocenters kept migrating initially northwest (P1 to P3) and then west (P3 to P6).
· The Salt Valley and Onion Creek salt walls are linked, as suggested by their surface bending geometries, which were inherited by the geometry of the preexistent adjacent depocenters.
· The first complete evacuation of salt associated with the Salt Valley salt wall occurred at the end of Cutler deposition and to the east of the wall. Later, this weld zone would expand radially, until the end of Chinle time when the present-day configuration of welds was reached on both flanks.
· Salt area, which is equal to the integrated thickness, in regional cross sections diminished by around 30% from the original depositional area. This assumes, as a first approximation, no movement of salt in or out of the plane of the cross sections. It is likely that most of salt area decrease was caused by dissolution, because salt was exposed at the surface for more than 20 million years.
· The highest rates of sediment accumulation, salt wall growth, salt evacuation (in welded areas), salt area decrease, and subsidence occurred during Cutler time, when the Uncompahgre Uplift was most active.
·
Depending
on the
· Based on this study, a number of different kinds of play concepts can be considered for oil exploration: carbonate-derived sandstones within the Paradox and Honaker Trail formations against the Uncompahgre Uplift, karstified carbonates in the Honaker Trail Formation adjacent to the salt walls, carbonate-derived sandstones in basal Cutler, adjacent to salt walls, and onlap of White Rim Sandstone against the Salt Valley salt wall and Cutler Group.
Doelling, H.H., 2001, Geologic map of the Moab and eastern part of the San Rafael Desert 30’ x 60’ Quadrangles, Utah Geological Survey Map 180, scale 1:100,000. Frahme, C.W. and E.B. Vaughn,
1983, Paleozoic geology and Ge, H., 1996, Kinematics and dynamics of
salt tectonics in the Paradox Basin, Utah and Colorado: field observations and
scaled Trudgill, B.D., N. Banbury and J.R. Underhill, 2004, Salt evolution as a control on structural and stratigraphic systems: northern Paradox foreland basin, SE Utah, USA, in GCSSEPM 24th Annual Research Conference.
Copyright © AAPG. Serial rights given by author. For all other rights contact author directly. |
