nd the “Pre-Illinois” and “Bedrock” were combined.
The next step was identifying the surface elevations for all of the wells. Using ESRI’s ArcGIS, a Digital Elevation Map (DEM) acquired from the ISGS Geospatial Data Clearinghouse, four quadrangle maps, and a layer created with the well locations were incorporated into a GIS database. The well layer was created by making a spreadsheet of all of the wells that were be used for the model. API and X, Y data (in UTM format) were included for each well. A surface elevation for each well was determined and incorporated into the well database.
The well data were sorted into separate spreadsheets such that each of the five lithostratigraphic sections had their own spreadsheet. These sections only included the top of each lithostratigraphic unit from each well to create well top data. These well top spreadsheets included the API, X, Y locations, elevation, and lithology.
Using Petrel, a new project was created with five sets of “well tops” folders. Each layer (Cahokia, Peoria, Wisconsin, Illinois, and Bedrock) was imported into their corresponding well top folder, which in Petrel are represented as a series of dots that make up the well layers (Figure 4). Each unit was created as a separate layer to ease subsequent editing/adjustment. Next, surfaces were created out of the well top data to generate the model (Figure 5) for the Cahokia, Peoria, Wisconsin, Illinois, and Bedrock (Table 1).
Figure 4. Petrel well top data for initial 3D model.
Figure 5. Geologic horizons interpreted by Petrel for initial model from well top data.
Table 1. Key to geology and axes for all Petrel screenshots.
2.4. Groundwater Flow Model
To establish and confirm hydrogeologic boundary conditions for the local (shallow) groundwater flow model, GFLOW  , an analytical element method was used to simulate regional flow through the surficial deposits comprised of diamicton tills and sand and gravel layers that total 15 m in thickness. On the regional scale the hydraulic conductivity (K) was assumed to be homogeneous and isotropic. The Sangamon River, to the east, Spring Creek, to the west, and Lake Decatur, along the east and southeast edge of the domain were near-field elements represented as constant head (Dirichlet) conditions. Model parameters were measured on site, calibrated by the model, or estimated using data acquired from the ISGS exploratory holes (Table 2). An initial simulation was conducted with GFLOW to establish regional flow and to aid in the development of local flow conditions (Figure 6).
The local groundwater flow model was developed using MODFLOW  . Using a uniform 0.15 km x 0.15 km cell (0.23 km2), a 40 row × 40 column grid represented the domain (Figure 7). Aquifer parameters and conditions used in the GFLOW model, with the exception of K, were used for the MODFLOW development. Rather than the 12 m/day, the local model calibrated to a K value of 0.12 m/day. The boundary conditions for the model domain were represented as constant heads, with values established from the GFLOW simulation (Figure 6). Spring Creek, Sangamon River, and Lake Decatur were also incorporated into the domain as constant head cells. Head values for Lake Decatur were obtained from a gauging station about 2 km downstream of the study area. (Haring, Pers. Com.). Recharge for the simulation was set at 10% (0.101 m/yr) of the average annual precipitation rate for Decatur, Illinois of 1.01 m/yr  . The use of 10% is consistent with other groundwater flow simulations in central Illinois.
Particle tracking, using MODPATH  , was used to further delineate the location of a groundwater divide identified with the GFLOW simulation (Figure 6). The horizontal migration was simulated by centering particles on the injection site and forward modeling. The time for the first particle to reach Lake Decatur signified the travel time.
Figure 6. GFLOW model of the area with flow lines in gray. Also shows Lake Decatur and the sequestration injection site.
Figure 7. The 40 × 40 MODLFOW grid over study area with boundary conditions included. Blue cells represent constant head conditions. Black cells are inactive cells. Gray circle represents the location of the sequestration site.
Table 2. Parameters used for GFLOW model.
3.1. Geologic Model
The Petrel model simulates Quaternary deposits overlying Pennsylvanian bedrock in the Decatur area, indicating glacial sediment thicknesses up to 50 m (Figure 8 & Figure 9). The Peoria Silt thins to the northwest and to the east where the lake is present. The resistive Wisconsin till is responsible for creating higher slopes along the east and west edges of the Lake (Figure 8). The Peoria Silt terminates at the top of these slopes along the western boundary of Lake Decatur and picks up along the flat lying areas west of the lake. Waters of the Sangamon River completely eroded the Wisconsin till unit beneath the lake and exposed the lower Illinois till. Fluvial processes associated with the Sangamon River have deposited a thin layer of Cahokia Alluvium within the floodplain and along the bottom of Lake Decatur where the Peoria silt and Wisconsin till units had previously been deposited.
The surface layer of the geologic model (Figure 6) includes the Cahokia alluvium, which is present in the streambed, the Peoria Silt, representing about 85% of the surface deposits, the Wisconsin till, occurring along the lake edges and in the northwest and east corners of the modeling area, and the Illinois till, which is present below the thin Cahokia alluvium in the lake bed. The Petrel model of the surficial geology is consistent with the published surficial geology map of the area  .
3.2. Groundwater Flow Model
The local groundwater flow model identified a NE-SW trending groundwater divide in the northwestern portion of the domain (Figure 10). Flow on the northern side of the divide is to the northwest, and flow along the southern side of the divide is to the southeast. The model simulated groundwater flow at the injection site would move to the southeast towards Lake Decatur. The forward modeling with MODPATH indicated that the particles placed at the injection site reached Lake Decatur in 80 days.
While Petrel is used mainly for subsurface modeling of continuous stratigraphic units in the petroleum and gas industry, this project indicates that Petrel has the capability to model discontinuous Quaternary units. To address the problem of modeling discontinuous units, a stratigraphic column consistent across all wells is needed; thus, an absent unit in a well is assigned a thickness of zero (0) meters. Where this occurs, the model result is a pinch out of the unit, excluding it accordingly. The modeling process in Petrel also required simplification (i.e. upscaling) of the Quaternary units because they are heterogeneous, with discontinuous lenses of sediments of various size, i.e. sand and gravel lenses. While Petrel is capable of distinguishing facies within units given high resolution log data   , the discontinuous nature of the lenses may be too detailed to model accurately. We did not address this issue. Rather, we modeled the materials on a unit/formation level (low resolution), homogenizing the units, instead of at the facies level. This simplified the model and produced fewer layers. The standard input procedures were also altered in order to model the Quaternary units. An additional method deviation was importing surfaces of well top data separately rather than collectively. This method allowed alterations of surfaces to be more efficient; if a surface needed to be altered, which it did frequently, only one layer was modified rather than the entire model.
A concern for broader project is that there are thick sand and gravel bodies within the glacial deposits or frac-
Figure 8. Plan view of the final Petrel model illustrating the surficial geology. The black circle is the estimated extent of the gas plume once it is injected and red dots show well distribution. Contour interval is 5 meters.
Figure 9. Petrel generated (a) east-west cross section along the southern margin of the geologic model (4412800 line); (b) east-west cross section along the 4415200 line of the geologic model.
Figure 10. Average head values are in red (contoured in feet). Projected gas plume at depth is the gray circle. The red X marks the position of the injection well. Results of the average flow MODPATH simulation with particles and flow paths in purple. This represents the position of the particles after 80 days.
tures in the bedrock surface that may act as significant migration pathways for gas if there is a shallow leak or if gas migrates vertically from deeper in the bedrock units. It is assumed that the overlying till can act as a cap layer given the combined thickness of the glacial units and the overall composition as being fine-grained, poorly sorted and believed to possess a low permeability and porosity. However, the unweathered till can have significant vertical and horizontal fracture permeability that will allow migration  . Additionally, all glacial till units have extensive lenses of sand and gravel that can act as lateral and/or vertical migration pathways.
Fluid flow in the shallow subsurface will be transported towards Lake Decatur. Any vertical leakage from the deep saline reservoir would take years, if not 100s of years, based upon vertical fluid migration from an oil and gas field  . Additionally, the successful injection of nearly 1,000,000 tons of CO2  reveals the feasibility of the reservoir. However, once in the glacial sediment, migration to the lake would be on the order of 10s to 100s of days. Since glacial units vary in composition such as the presence of discontinuous sand and gravel lenses, flow rates through the units will vary as compared to the model. However, the general direction of groundwater flow will remain the same, towards Lake Decatur.
Petrel is used traditionally for subsurface modeling of deep, continuous bedrock systems by the petroleum and gas industry. This project successfully tested the program’s ability to model discontinuous Quaternary units. To combat this problem of modeling discontinuous units, a consistent stratigraphic column across all wells was used to so where a unit was absent in a well, it was included with a thickness of 0’. Using this method, a successful geologic model was created with stratigraphic units pinching out as needed honoring the well data. The Quaternary units also had to be simplified in order for the Petrel modeling process to work. Since there are mostly till deposits above bedrock in this area with a thin layer of loess on the surface, modeling was from a somewhat low resolution. Any sand deposit encountered in a well log less than 0.67 m thick was combined with the surrounding material. This simplified the facies within the major till units resulting in a simplified model with fewer layers. The standard Petrel model input procedures were also altered in order to map the Quaternary units. Well top data were imported as separate stratigraphic surfaces rather than being associated with individual wells resulting in the seamless ability to alter or edit surfaces as needed. Overall it can be concluded that Petrel has the ability to model discontinuous geologic units.
The resulting model is an accurate representation of Quaternary deposits in the Decatur area. They are up to 48 m thick in some places and thinner or eroded completely where Lake Decatur has cut through. The Peoria Silt covers most of the surface except on the topographic high slopes along the edges of Lake Decatur. In these places, the Wisconsin till is present along with the flat, higher areas in the northwest corner of the mapping area. The Cahokia alluvium fills in the streambed of Lake Decatur where it has completely eroded the Peoria Silt and Wisconsin till deposits. The geometry of the Quaternary units in this area is somewhat simple, though the composition is mostly consistent.
 White, D., et al. (2004) Greenhouse Gas Sequestration in Abandoned Oil Reservoirs: The International Energy Agency Weyburn Pilot Project. GSA Today, 14, 4-10.
 Petroleum Technology Research Centre (2015) Weyburn-Midale: The IEAGHG Weyburn-Midale CO2 Monitoring and Storage Project.
 Statoil (2015) Technology & Innovation.
 Arts, R., et al. (2004) Monitoring of CO2 Injected at Sleipner Using Time-Lapse Seismic Data. Energy, 29, 1383-1392.
 Midwest Geological Sequestration Consortium (2016) Deep Saline Storage.
 Preston, C., et al. (2005) IEA GHG Weyburn CO2 Monitoring and Storage Project. Fuel Processing Technology, 86, 1547-1568.
 Wells, A.W., et al. (2007) The Use of Tracers to Assess Leakage from the Sequestration of CO2 in a Depleted Oil Reservoir, New Mexico, USA. Applied Geochemistry, 22, 996-1016.
 Peterson, E.W., Martin, L.I. and Malone, D.H. (2015) Identification of Potential Vertical Gas Migration Pathways above Gas Storage Reservoirs. World Journal of Environmental Engineering, 3, 23-31.
 Lovelace, B. (2008) Can We Protect Our Ground Water If We Deploy Large-Scale Carbon Sequestration Technologies? Ground Water, 46, 805-806.
 Pruess, K. (2008) On CO2 Fluid Flow and Heat Transfer Behavior in the Subsurface, Following Leakage from a Geologic Storage Reservoir. Environmental Geology, 54, 1677-1686.
 Blendinger, W., Brack, P., Norborg, A.K. and Wulff-Pedersen, E. (2004) Three-Dimensional Modelling of an Isolated Carbonate Buildup (Triassic, Dolomites, Italy). Sedimentology, 51, 297-314.
 Wagle, J., Malone, D.H., Peterson, E. and Tranel, W.L. (2016) Porosity Controls on Secondary Recovery at the Loudon Field, South-Central Illinois. Interpretation, 4, T1-T13.
 Carlock, D.C., Thomason, J.F., Malone, D.H. and Peterson, E.W. (2016) Stratigraphy and Extent of the Pearl-Ashmore Aquifer, McHenry County, IL, USA. World Journal of Environmental Engineering, 4, 6-18.
 Kimple, D., Peterson, E.W. and Malone, D.H. (2015) Stratigraphy and Porosity Modeling of Southern Central Illinois Chester (Upper Mississippian) Series Sandstones Using Petrel. World Journal of Environmental Engineering, 3, 82-86.
 Hansel, A.K. and Johnson, W.H. (1996) Wedron and Mason Groups: Lithostratigraphic Reclassification of Deposits of the Wisconsin Episode, Lake Michigan Lobe Area. Illinois State Geological Survey, Champaign.
 Kempton, J.P., Morse, W.J. and Visocky, A.P. (1982) Hydrogeologic Evaluation of Sand and Gravel Aquifers for Municipal Groundwater Supplies in East-Central Illinois. Illinois State Water Survey and the Illinois State Geological Survey.
 Illinois State Geological Survey (2015) Illinois Water Well (ILWATER) Interactive Map.
 Illinois State Geological Survey (2015) Coal Mines in Illinois Viewer (ILMINES).
 McDonald, M.G. and Harbaugh, A.W. (1988) A Modular Three-Dimensional Finite-Difference Ground-Water Flow Model. Techniques of Water-Resources Investigations of the United States Geological Survey, United States Geological Survey, Washington DC.
 Pollock, D.W. (1994) User’s Guide for MODPATH/MODPATH-PLOT. Version 3: A Particle Tracking Post-Processing Package for MODFLOW, the US Geological Survey Finite-Difference Ground-Water Flow Model.
 Keller, C.K., Kamp, G.V.D. and Cherry, J.A. (1986) Fracture Permeability and Groundwater Flow in Clayey Till Near Saskatoon, Saskatchewan. Canadian Geotechnical Journal, 23, 229-240.
 Weaver, T.R., Frape, S.K. and Cherry, J.A. (1995) Recent Cross-Formational Fluid Flow and Mixing in the Shallow Michigan Basin. Geological Society of America Bulletin, 107, 697-707.