| 2.1 Has required elements: nonspatial tables DataSources, DescriptionOfMapUnits, GeoMaterialDict; feature dataset GeologicMap with feature classes ContactsAndFaults and MapUnitPolys | PASS |
| 2.2 Required fields within required elements are present and correctly defined | PASS |
| 2.3 All MapUnitPolys and ContactsAndFaults based feature classes obey Level 2 topology rules: no internal gaps or overlaps in MapUnitPolys, boundaries of MapUnitPolys are covered by ContactsAndFaults | PASS |
| 2.4 All map units in MapUnitPolys have entries in DescriptionOfMapUnits table | PASS |
| 2.5 No duplicate MapUnit values in DescriptionOfMapUnit table | PASS |
| 2.6 Certain field values within required elements have entries in Glossary table | PASS |
| 2.7 No duplicate Term values in Glossary table | PASS |
| 2.8 All xxxSourceID values in required elements have entries in DataSources table | PASS |
| 2.9 No duplicate DataSources_ID values in DataSources table | PASS |
| 3.1 Table and field definitions beyond Level 2 conform to GeMS schema | PASS |
| 3.2 All MapUnitPolys and ContactsAndFaults based feature classes obey Level 3 topology rules: No ContactsAndFaults overlaps, self-overlaps, or self-intersections. | PASS |
| 3.3 No missing required values | PASS |
| 3.4 No missing terms in Glossary | PASS |
| 3.5 No unnecessary terms in Glossary | PASS |
| 3.6 No missing sources in DataSources | PASS |
| 3.7 No unnecessary sources in DataSources | PASS |
| 3.8 No map units without entries in DescriptionOfMapUnits | PASS |
| 3.9 No unnecessary map units in DescriptionOfMapUnits | PASS |
| 3.10 HierarchyKey values in DescriptionOfMapUnits are unique and well formed | PASS |
| 3.11 All values of GeoMaterial are defined in GeoMaterialDict. GeoMaterialDict is as specified in the GeMS standard | PASS |
| 3.12 No duplicate _ID values | PASS |
| 3.13 No zero-length, whitespace-only, or bad null values | PASS |
| MapUnit | DescriptionOfMapUnits | CrossSectionA | GeologicMap | CorrelationOfMapUnit |
|---|---|---|---|---|
| Kmp | X | X | X | X |
| Xu | X | X | -- | X |
| Qaco | X | -- | X | X |
| af | X | -- | X | X |
| Qeo | X | -- | X | X |
| Qac | X | -- | X | X |
| Qc | X | -- | X | X |
| water | X | -- | X | -- |
| Kml | X | X | -- | X |
| Qa | X | -- | X | X |
| Kms | X | X | X | X |
| Qamf | X | -- | X | X |
| Qaf1 | X | -- | X | X |
| Qg1 | X | -- | X | X |
| Qaf4 | X | -- | X | X |
| Qg3 | X | -- | X | X |
| Qco | X | -- | X | X |
| Jm | X | X | -- | X |
| Kdb | X | X | -- | X |
| Qaf5 | X | -- | X | X |
| Mz | X | X | -- | X |
| Qg2 | X | -- | X | X |
| Qaf2 | X | -- | X | X |
| Qaf3 | X | -- | X | X |
| Qaf7 | X | -- | X | X |
| Qaf6 | X | -- | X | X |
| Kmu | X | X | X | X |
| OBJECTID | Source | Notes | URL | DataSources_ID |
|---|---|---|---|---|
| 9 | Baylor Geoluminescence Dating Resarch Lab | None | https://geosciences.artsandsciences.baylor.edu/about-us/facilities/geoluminescence-dating-research-lab | BAYLOR1 |
| 2 | This study | None | None | DAS1 |
| 5 | Online dictionary | None | https://dictionary.com/ | DICT1 |
| 6 | Colorado Division of Water Resources | None | https://dwr.colorado.gov/ | DWR1 |
| 7 | Energy and Carbon Management Commission | None | https://ecmc.state.co.us/#/home | ECMC1 |
| 1 | Federal Geographic Data Committee [prepared for the Federal Geographic Data Committee by the U.S. Geological Survey], 2006, FGDC Digital Cartographic Standard for Geologic Map Symbolization: Reston, Va., Federal Geographic Data Committee Document Number FGDC-STD-013-2006, 290 p., 2 plates. | None | https://ngmdb.usgs.gov/fgdc_gds/geolsymstd.php | FGDC-STD-013-2006 |
| 4 | GeMS standard | None | https://ngmdb.usgs.gov/Info/standards/GeMS/ | GeMS1 |
| 3 | Online geologic dictionary | None | https://geology.com/geology-dictionary.shtml | GEODICT1 |
| 8 | US Geological Survey | None | https://www.usgs.gov | USGS1 |
| OBJECTID | MapUnit | Name | FullName | Age | Description | HierarchyKey | ParagraphStyle | Label | Symbol | AreaFillRGB | AreaFillPatternDescription | DescriptionSourceID | GeoMaterial | GeoMaterialConfidence | DescriptionOfMapUnits_ID |
|---|---|---|---|---|---|---|---|---|---|---|---|---|---|---|---|
| 1 | None | SURFICIAL DEPOSITS | SURFICIAL DEPOSITS | None | Map units are described using the following classifications: grain sizes from Wentworth (1922); thickness of bedding terms codified in the current classification of the Society for Sedimentary Geology (SEPM); and carbonate content of rock and calcic soils judged by intensity of effervescence (fizz or bubbling) that resulted from the application of 10% hydrochloric acid (HCl) to a rock or soil sample in the field. Pedogenic calcic soil development stages are from Machette (1985). Surficial deposits may include color classifications in parenthesis from the Globe pocket guide for the Identification of Soil Colors that uses the Munsell color system. | 01 | DMUHeading1 | None | None | None | None | DAS1 | None | None | DMU01 |
| 2 | None | HUMAN-MADE DEPOSITS | HUMAN-MADE DEPOSITS | None | None | 01.01 | DMUHeading2 | None | None | None | None | DAS1 | None | None | DMU02 |
| 3 | af | Artifical fill | Artifical fill | Uppermost Holocene | Gravel, sand, silt, and clay emplaced as fill to construct road, canal, and dam embankments, or any other human-made fills. The unit includes natural sediments and landfills composed of unknown materials. Fills may be engineered or uncontrolled. Their compositions and properties are varied. The unit locally may include disturbed land, excavations, overburden spoils related to landfill sites, and gravel or borrow pits. | 01.01.01 | DMUUnit1 | af | af | 255-255-255 | None | DAS1 | "Made" or human-engineered land | High | DMU03 |
| 4 | None | ALLUVIAL DEPOSITS | ALLUVIAL DEPOSITS | None | None | 01.02 | DMUHeading2 | None | None | None | None | DAS1 | None | None | DMU04 |
| 5 | Qa | Alluvium | Alluvium | Upper and Middle Holocene | Tan-gray, interlaminated to very thinly bedded, very fine to fine-grained sand and sandy to silty clay. The unit typically covers the floor of active drainage channels and swales within meanders incised in alluvial mudflow and mud-fan valley fill deposits (Qamf) and shale bedrock. Unit may locally contain pebble to boulder gravelly lenses. Rocks also typically litter gully floors, which are transported during flood events or by debris flows. The unit includes up to three meandering terrace deposits above the active channel floor. The lowest, from 1.5 m to 2 m above the channel floor, exhibits active surface flood scour morphology. This unit is susceptible to periodic flash flooding and deposition of debris flows. | 01.02.01 | DMUUnit1 | Qa | Qa | 255-255-115 | None | DAS1 | Alluvial sediment | High | DMU05 |
| 7 | None | Alluvial gravel deposits | Alluvial gravel deposits | None | Deposits are linear remnants of river terrace treads that approximate the longitudinal profile of the major creeks of the quadrangle: Prairie Canyon Creek, West Salt Creek, and East Salt Creek. These creek watersheds extend northward, off map, to valleys and canyons incised through the Book Cliffs into the Roan Plateau. The predominate deposit is a fluvial, sorted, and imbricated cobbly gravel with scattered small boulders (<1 m). Well-sorted sand lenses are locally present. Clasts are primarily sandstone; the provenance being Upper Cretaceous Mesa Verde Group (Iles and Williams Fork formations) and underlying marine sandstones of the upper part of the Mancos Shale exposed in the Book Cliffs. However, there are small amounts (<5%) of other lithologies including red-colored coal-fire clinker and pebbles composed of chert, petrified wood, and igneous and metamorphic rocks. These pebbles are reworked from terrestrial conglomeritic channels and beds within the Paleogene Ohio Creek and Wasatch formations exposed in the Roan Plateau above the Mesa Verde rocks. Cobble-sized sandstone clast shapes are low sphericity, but moderately to well rounded, with shapes ranging from bladed or slabby to discoid. Except for the lowest gravel (Qg1), the well sorted riverine deposits near the contact with the underlying Mancos Shale or finer-grained mud alluvium are commonly cemented to conglomerate that locally forms ledge-type outcrops along the terrace bluff. The deposit also locally contains muddy fine-grained interlaminated to thinly interbedded overbank deposits and channels that contain unsorted bouldery debris flow gravel in a muddy matrix. Alluvial deposits have been a historic gravel resources in the map area. | 01.03 | DMUHeading2 | None | None | None | None | DAS1 | None | None | DMU06 |
| 8 | Qg1 | Alluvial gravel one | Alluvial gravel one | Upper Pleistocene | Map unit forms broad fan-shaped mesas and isolated terrace remnants in the southern third of the map area. The top of the unit averages 18 m above base level. Gravel deposits are unconsolidated and are about 3 m thick. An abandoned gravel pit in this deposit exposed riverine pebbly to cobbly gravel near Old Highway 6&50 on the west bank of West Salt Creek near the confluence with Badger Wash. Unit thickness at the pit is about 2 m. | 01.03.01 | DMUUnit1 | Qg1 | Qg1 | 255-255-215 | 163-255-155 ESRI 24k Geology 605 Breccia | DAS1 | Alluvial sediment, mostly coarse-grained | High | DMU07 |
| 9 | Qg2 | Alluvial gravel two | Alluvial gravel two | early Upper Pleistocene | Gravel deposits beneath remnants of terrace surfaces are 26 m above the West Salt Creek. The terrace remnants extend to the northern map boundary. Where the deposit is well-sorted riverine gravel within the West Salt Creek valley, the unit is locally well cemented and forms a conglomerate. The durability of the conglomeritic gravel deposit locally prevents erosion of the adjacent shale slope such that deposits of subsequent sheetwash (unit Qaco) locally form low-gradient fans that lap onto the Qg2 unit. Thickness is variable, but maximum observed thickness is 11 m, which included overbank mud and sand sediments underlying the gravel. A clean riverine sand lens was sampled (BW-044 in age table on Plate 2) for optically stimulated luminescence (OSL) dating. The sample yielded a minimum age of >87,000 years before present (ybp), which suggests deposition during the Bull Lake glaciation (marine isotope stage MIS-5 and MIS-6). In old gravel pits, the thickness of the mined gravel is 3 m. | 01.03.02 | DMUUnit1 | Qg2 | Qg2 | 255-255-215 | 255-127-127 ESRI 24k Geology 605 Breccia | DAS1 | Alluvial sediment, mostly coarse-grained | High | DMU08 |
| 10 | Qg3 | Alluvial gravel three | Alluvial gravel three | Upper Pleistocene | Deposits of fluvial gravel beneath alluvial terrace surfaces form small mesas that overlie the Smoky Hill Member of the Mancos Shale (Kms) about 45 m above the base level. Deposits are near the southern margin of the map area in what was the paleo-confluence of East and West Salt Creeks. This unit correlates with the off-map deposit of Mack Mesa (Qam2 of White and others, 2015). In old gravel pits, the thickness of the gravel is up to 5 m. | 01.03.03 | DMUUnit1 | Qg3 | Qg3 | 255-255-215 | 99-167-255 ESRI 24k Geology 605 Breccia | DAS1 | Alluvial sediment, mostly coarse-grained | High | DMU09 |
| 36 | None | ALLUVIAL FAN AND MUDFLOW DEPOSITS | ALLUVIAL FAN AND MUDFLOW DEPOSITS | None | None | 01.04 | DMUHeading2 | None | None | None | None | DAS1 | Alluvial sediment, mostly fine-grained | High | DMU10 |
| 6 | Qamf | Alluvial mudflow and mud-fan deposits | Alluvial mudflow and mud-fan deposits | Holocene and Upper Pleistocene | Tan-gray, poorly to moderately sorted, interlaminated to very thinly bedded, unconsolidated, very fine to fine grained, silty to clayey sand. Unit includes Holocene terrace sediments of the modern drainage channels of major creeks and locally includes clay-, silt-, and sand-rich alluvium deposited by tributary streams, alluvial-fan, and hillside slopewash (chiefly sheetwash) sediments. The deposit is locally gravel-bearing; either clast-supported cross-bedded pebbly gravel or matrix-supported pebble gravel clasts dispersed in the deposit. Clasts are derived from reworking of older alluvial gravel and alluvial fan deposits (Qg and Qaf) near adjacent hills and mesas, and rare lenses of entrained cobbles and boulders deposited during floods or by debris flows. The pebble to small boulder (< 40 cm) gravel-sized clasts are predominantly from the Book Cliffs region north of the map area. Sample BW-189 (in age table on Plate 2) was taken 6.7 m below the terrace surface and 1.8 m above the active channel floor for OSL dating that yielded an estimated age of 12,755 ± 615 ybp. Total unit thickness at the sample site was 8.5 m, which is near the maximum thickness of the unit near the main trunk of the West Salt Creek valley (9 m). The unit locally thins to 2 m in broad alluvial fans and flatlands that overlying the Smoky Hill Member of the Mancos Shale (Kms). In southern parts of the map area overlying the Kms bedrock, the deposit locally is altered by agricultural tilling and may locally include shale bedrock residuum. The sediment of this unit may be prone to hydrocompaction settlement (White and Greenman, 2008), expansive (swelling) soils, and (or) dispersion upon wetting. Pseudokarst features such as fissures and small ground openings may be present locally. | 01.04.01 | DMUUnit1 | Qamf | Qamf | 255-255-190 | None | DAS1 | None | None | DMU11 |
| 11 | None | Alluvial fan deposits | Alluvial fan deposits | None | Forms aggraded, gently-sloping, alluvial fans that may (locally?) become constrained (and narrow to form?) stream-terrace deposits. More resistant to erosion than the surrounding shale, the units are topographically inverted; subdivided and enumerated based on height of remnant gravel-capped mesas, hilltops, and narrow ridges above modern stream level. Unconsolidated deposits range from very bouldery, unsorted, non-stratified, matrix-supported, gravelly debris-flow deposits to better-sorted, stratified, clast-supported, imbricated, sandy, cobbly gravel deposited by fluvial processes. Clasts are angular to subrounded slabby sandstone that were eroded by the incision of steep-walled gulches cut into the Book Cliffs. Deposits may locally contain boulder levees and channel fill that record debris-flow events. Older units typically have thin mantles composed of light red (Munsell 2.5YR 7/8) loess (< 1m thick) reworked and redeposited chiefly by sheetflow. Unit supports more dense vegetation than the adjacent Mancos Shale. Heights recorded are those of the deepest nearby drainage channels or elevation (m) above mean sea level (AMSL). | 01.04.02 | DMUHeading2 | None | None | None | None | DAS1 | None | None | DMU12 |
| 12 | Qaf1 | Alluvial fan deposits one | Alluvial fan deposits one | Lower Holocene and Upper Pleistocene | Unit forms low fan and fan remnants adjacent to hills composed of Mancos Shale. Thickness is unknown, but young gullies of Upper Holocene age are incised 3 m into the unit. | 01.04.02.01 | DMUUnit1 | Qaf1 | Qaf1 | 255-255-190 | 112-168-0 ESRI 24k Geology 607 sand | DAS1 | Alluvial sediment, mostly coarse-grained | High | DMU13 |
| 13 | Qaf2 | Alluvial fan deposits two | Alluvial fan deposits two | Upper Pleistocene | Unit forms low-level alluvial fans that extend down from the Book Cliffs to form Qg2 terrace gravel where the valley is constrained by the Prairie Canyon Member of the Mancos Shale (Kmp). Unit is locally mantled with patchy red (Munsell 2.5YR 7/8) silty to very-fine-grained sandy loess. The top of the unit is about 26 m above the creek floor and is 4.5 to 9 m thick. | 01.04.02.02 | DMUUnit1 | Qaf2 | Qaf2 | 255-255-190 | 255-0-197 ESRI 24k Geology 602 gravel | DAS1 | Alluvial sediment, mostly coarse-grained | High | DMU14 |
| 14 | Qaf3 | Alluvial fan deposits three | Alluvial fan deposits three | Upper Pleistocene | Unit contains widespread alluvial fans remnants at an approximate elevation of 1,585 m AMSL in the central part of the map area near the northern boundary. Fan surface typically is thinly mantled (<1 m) by reworked, red (Munsell 2.5YR 7/8), loess-rich, sheetwash deposits. Unit has a poorly exposed Bk soil horizon. Clasts exposed at the surface are partially covered with calcic coatings, which likely have Stage II calcic development (Machette, 1985). Unit thickness is variable, but likely does not exceed 3 m. Top of unit Qaf3 is about 15 m above the Qaf2 surface. | 01.04.02.03 | DMUUnit1 | Qaf3 | Qaf3 | 255-255-190 | 0-112-255 ESRI 24k Geology 602 gravel | DAS1 | Alluvial sediment, mostly coarse-grained | High | DMU15 |
| 15 | Qaf4 | Alluvial fan deposits four | Alluvial fan deposits four | Upper Pleistocene | Unit forms isolated mesas and ridgelines near the map's northern boundary at an intermediary elevation between the more widespread Qaf3 surfaces and Qaf5 surfaces. Surface of unit Qaf4 is thinly mantled with reworked red (Munsell 2.5YR 7/8) loess. Clasts are typically slabby subangular sandstone clasts eroded from the nearby Book Cliffs and typically have calcic coatings where exposed. Deposit surface is 27 m above the local drainage channel. Top of unit Qaf4 is about 7 m above the top of unit Qaf3. | 01.04.02.04 | DMUUnit1 | Qaf4 | Qaf4 | 255-255-190 | 255-0-0 ESRI 24k Geology 602 gravel | DAS1 | Alluvial sediment, mostly coarse-grained | High | DMU16 |
| 16 | Qaf5 | Alluvial fan deposits five | Alluvial fan deposits five | upper Middle Pleistocene | Unit occurs as a discontinuous belt of alluvial fan remnants capping isolated hilltops and narrow ridgelines that overlie Mancos Shale near the northeast corner of the map area. Deposit surface elevation at the north map boundary is 1,632 m AMSL and declines to 1,528 m over a 3.7 km distance. A northwest to southeast slope gradient is 28 m/km. The top of unit Qaf5 is about 15 m above the top of unit Qaf4. | 01.04.02.05 | DMUUnit1 | Qaf5 | Qaf5 | 255-255-190 | 76-230-0 ESRI 24k Geology 602 gravel | DAS1 | Alluvial sediment, mostly coarse-grained | High | DMU17 |
| 17 | Qaf6 | Alluvial fan deposits six | Alluvial fan deposits six | upper Middle Pleistocene | Unit occurs as remnants of fan gravel that contains small boulders composed of sandstone that caps isolated hilltops and narrow ridgelines underlain by Mancos Shale in the upper margin of the northeast quadrant of the quadrangle. Unit is less than 2 m thick and Mancos Shale residuum is locally exposed at the surface. The southward slope gradient of this alluvial fan surface is 66 m/km. The unit surface elevation is about 10 m above that of unit Qaf5. The surface elevation of unit Qaf6 is like that of the Qaf7 unit near the northern map boundary. However, the steeper gradient places the southern remnants of unit Qaf6 at a lower elevation of unit Qaf7. | 01.04.02.06 | DMUUnit1 | Qaf6 | Qaf6 | 255-255-190 | 168-168-0 ESRI 24k Geology 602 gravel | DAS1 | Alluvial sediment, mostly coarse-grained | High | DMU18 |
| 18 | Qaf7 | Alluvial fan deposits seven | Alluvial fan deposits seven | Middle Pleistocene | This conspicuous unit occurs along the west side of the map area and forms high mesas from the north boundary to the south boundary of the quadrangle. Unit consists of heterogeneous alluvial deposits composed of interlaminated silty to sandy clay that is capped by well sorted, imbricated, riverine cobbly gravel that is well-cemented. The latter forms a resistant conglomerate bed that forms a vertical bluff that caps the mesa. The underlying interlaminated alluvial mud beds show evidence of load deformation. The upper conglomerate is well exposed in a vertical bluff along mesa edges. The unit is 15 m thick where the mud unit is exposed. At the location of an old gravel pit in the southwest corner of the map area, the muddy alluvium is not present, and the riverine conglomerate is only 5 m thick. The Lava Creek B tephra (~631 ka, MIS Stage 16-15, dated by Matthews and others (2015)) was not seen in the map area, but was reported in this same unit at two nearby locations on the Bar X Wash quadrangle, 2 km and 4.7 km west of the west map boundary, on each side of Prairie Canyon (written communication, Andres Aslan, Colorado Mesa University, Sept 11, 2008; written communication, Rex Cole, Colorado Mesa University (retired), March 21, 2023). The tephra is in the lower alluvial mud beds below the conglomerate. Unit Qaf7 is about 122 m above the floor of the adjacent Prairie Canyon. Deposit surface in the northwestern part of the map area is 1,617 m AMSL and declines to 1,518 m over a distance of 12.7 km, a north to south downslope gradient of 8 m/km. The surface of the high mesa is mantled with fine-grained red soil (Munsell 2.5YR 6/8) above a ~1 m thick carbonate-rich K horizon that is exposed along the mesa rim. The K horizon likely has stage III+ to IV calcic soil development (Machette, 1985). | 01.04.02.07 | DMUUnit1 | Qaf7 | Qaf7 | 255-255-190 | 190-210-255 ESRI 24k Geology 602 gravel | DAS1 | Alluvial sediment, mostly coarse-grained | None | DMU19 |
| 19 | None | EOLIAN DEPOSITS | EOLIAN DEPOSITS | None | None | 01.05 | DMUHeading2 | None | None | None | None | DAS1 | None | None | DMU20 |
| 20 | Qeo | Old eolian deposits | Old eolian deposits | Upper Pleistocene | Light red to orange-red (Munsell 10YR 6/8 to 2.5YR 7/8) silt, clay, and very fine-grained sand that thinly mantle two gentle slopes underlain by Mancos Shale. Unit was deposited by wind and was reworked by slope processes. Reddish hues may be (likely?) related to soil development. Local chalky-colored exposures along slopes are formed by erosion and exposure of well-developed Bk soil horizons. Very thin deposits (<1 m) and discontinuous mantles of loess on the surfaces of older Qg units, older Qaf units, and unit Qaco were not mapped. Unit Qeo has more extensive vegetation cover than the surrounding hills composed of Mancos Shale. Unit thickness is generally less than 2 m. | 01.05.01 | DMUUnit1 | Qeo | Qeo | 230-230-0 | None | DAS1 | Eolian sediment | High | DMU21 |
| 21 | None | ALLUVIAL AND COLLUVIAL DEPOSITS | ALLUVIAL AND COLLUVIAL DEPOSITS | None | None | 01.06 | DMUHeading2 | None | None | None | None | DAS1 | None | None | DMU22 |
| 22 | Qac | Alluvial and colluvial deposits, undivided | Alluvial and coluvial deposits, undivided | Holocene | Tan-gray, unconsolidated, poorly sorted to unsorted silt, clay, and sand that is primarily deposited on hillsides and in swales chiefly by sheetwash and mass-movement processes. The deposit locally may contain abundant sandstone chips where sediment is derived from the Prairie Canyon Member of the Mancos Shale (Kmp), or large dispersed pebbles, cobbles, and small boulder-sized sandstone clasts where the sediment is derived from the erosion of older gravel that cap adjacent mesa remnants. Thickness is highly variable and likely does not exceed 2 m. | 01.06.01 | DMUUnit1 | Qac | Qac | 215-215-158 | 255-0-197 ESRI 24k Geology 601 gravel | DAS1 | Alluvial sediment, mostly fine-grained | High | DMU23 |
| 23 | Qaco | Old alluvial and colluvial deposits, undivided | Old alluvial and colluvial deposits, undivided | Upper to Middle Pleistocene | Reddish tan, unconsolidated, silt, clay, and sand with lesser amounts of dispersed, matrix-supported, pebble-sized clasts as well as scattered cobbles and small boulders (<0.5 m) reworked from adjacent and higher older deposits of Qg and Qaf. Deposit may locally contain abundant sandstone disc-shaped chips (up to 1 cm thick and 6 cm wide). Deposits are poorly sorted and very weakly stratified. Sandstone-chip clasts are of local upslope origin (unit Kmp). The deposit accumulated on gentle to moderate slopes (≤10°, but averaging about 4°) where wind and sheetwash processes predominate. Unit forms thin mantles where shale slopes abut against deposits of Qg and Qaf, and atop relict hillside fan surfaces. Unit Qaco locally includes reworked red (Munsell 2.5YR 7/8) loess, and clay and sandstone-chip residuum from slope-derived sediments eroded from unit Kmp bedrock. Exposures are poor, but a chalky-white band along slope breaks are due to a Bk soil horizon. Soil development, reddish hue, and elevation above the adjacent stream levels indicate a late to middle Pleistocene age for the unit. Unit thickness likely does not exceed 2 m. Mancos Shale bedrock residuum may be locally exposed in the unit. | 01.06.02 | DMUUnit1 | Qaco | Qaco | 255-255-115 | 230-0-0 ESRI 24k Geology 605 breccia | DAS1 | Alluvial sediment, mostly coarse-grained | High | DMU24 |
| 24 | Qc | Colluvial deposits | Colluvial deposits | Holocene | Tan-gray, unsorted, non to very poorly stratified, cobbly gravel-sized rock fragments with minor boulders (<1 m) deposited primarily by gravity on and along the base of steeper slopes near the angle of repose (≤34°). Deposits generally underlie older Qaf-mantled mesas and ridgelines and may locally include conglomerate blocks (eroded from what unit?) down slope of older gravel-capped mesas where conglomeratic intervals outcrop. Deposit has an unsorted clayey sandy matrix that was transported by overland sheet flow that transported relatively fine-grained material. Unit thickness is variable, but is likely less than 3 m. | 01.06.03 | DMUUnit1 | Qc | Qc | 255-235-175 | None | DAS1 | Colluvium and other widespread mass-movement sediment | High | DMU25 |
| 34 | Qco | Older colluvial deposits | Older colluvial deposits | Upper to Middle Pleistocene | Unit description is similar to Qc deposits described above, but is older. The rocks in these older, thin colluvial deposits armor shale slopes so that they are more resist to erosion. Differential erosion rates of the shale bedrock and armored surfaces underlain by unit Qco alter the normally uniform shale hillslopes, creating flatiron-shaped facets or irregular slopes below older Qaf deposits that cap the mesas. Deposit typically has a Bk soil horizon and clasts that are exposed in the unit have calcic coatings. Unit thickness is variable, but typically is about 2 m. Shale bedrock residuum may be locally exposed within the unit. | 01.06.04 | DMUUnit1 | Qco | Qco | 254-249-194 | 255-127-127 10% ordered stipple | DAS1 | Colluvium and other widespread mass-movement sediment | High | DMU26 |
| 25 | None | BEDROCK GEOLOGY | BEDROCK GEOLOGY | None | Surface bedrock of the Badger Wash quadrangle is composed of upper members of the Mancos Shale. The Mancos Shale in the Badger Wash area contains lithologic unit names that are transitional from Colorado to Utah. Historically, units of the Mancos Shale in Utah have been mapped in northwest Colorado south of the Uinta Basin and into the Grand Valley (Molenaar and Cobban, 1991; Cole and others, 1997). The units used in this map reflects lithostratigraphic and biostratigraphic work by the U.S. Geological Survey (Merewether and others, 2006; Ball and others, 2010); as well as recent work by the CGS reported in 1:24,000-scale geologic maps in the nearby Grand Valley, Whitewater, and Delta quadrangles (Livaccari and Hodge, 2009; White and others, 2014; White, 2014; Noe and others, 2015; and White and others, 2015). The recent work correlate coeval informal units of the Mancos Shale with Pierre Shale equivalents along the Front Range as well as with those of Mancos-Mesa Verde National Park area in southwestern Colorado (Leckie and others, 1997). The equivalent Utah Mancos members mapped near the state border (Gualtieri, 1988; Willis, 1994; Cole and others, 1997) are shown below in parentheses. The shale, where exposed, typically contains thin bentonite beds and is heavily fractured and contains fracture fillings composed of secondary gypsum (selenite). Expansive clay minerals promote swelling-soil hazards in shale bedrock as well as in their derived sediments. The "fat" clay (high plasticity) soils become greasy, cohesive, and clump when wetted, making walking and vehicle access difficult. | 02 | DMUHeading1 | None | None | None | None | DAS1 | None | None | DMU27 |
| 26 | Kmu | Upper part of the Mancos Shale (upper Blue Gate Member) | Upper part of the Mancos Shale (upper Blue Gate Member) | Upper Cretaceous | Dark gray to gray black, non-calcareous, broadly banded shale. The shale is finely fissile where weathered, but with depth the shale in outcrop becomes blocky or sub-blocky. Bentonite beds and secondary crystalline gypsum are common. Orange-brown dolomite concretion horizons occur; some are fossiliferous; some individual concretions as large as 2 m in diameter. The lower part of the unit becomes increasingly gray-black and bentonitic. Lowest strata of Unit Kmu is lithostratigraphically equivalent to the Sharon Springs Member as mapped in the North Delta quadrangle (Noe and others, 2015). Basal contact with unit Kms is marked by a downward color change in the shale from gray-black to tan-gray, the common presence of sandstone lamina, and two concretionary horizons just below (~4 m) the top of the Kmp unit. Where exposed, the gray-black shale of unit Kmu typically weathers at the surface to very light gray compared to the more tan-gray, sandy Kmp Member. This Kmu unit does not correlate with the Kmu unit (lower undivided members of the Mancos Shale) of Livaccari and Hodge (2009) in the nearby Fruita quadrangle. Unit Kmu is about 427 m thick. | 02.01 | DMUUnit1 | Kmu | Kmu | 170-198-129 | None | DAS1 | Mostly mudstone | High | DMU28 |
| 27 | Kmp | Prairie Canyon Member | Prairie Canyon Member | Upper Cretaceous | Tan-gray to dark-gray, non-calcareous, silty to sandy shale and interlaminated to thinly interbedded, very fine to fine-grained, non- to slightly calcareous sandstone. Thin lenticular to flaser bedding is common. Lenticular sandstone lamina chips typically litter hill slopes; some have wavy pinch-and-swell structure and ichnofossils. A typical sandstone chip is less than 1 cm thick and 6 cm wide, but sandstone beds up to 7 cm thick occur. Unit contains thin bentonite seams and resistant, planar, <1-m thick, orange-brown ferrous dolomite beds. The concretionary dolomite beds have lumpy bases and are laterally discontinuous. These beds are well indurated compared to the sandy shale. They are resistant to weathering and typically form low cuestas and (or) dipslope hillsides. From a type section measured and described in part in Badger Wash map area, Cole and others (1997) formally described this Mancos Shale Member, previously referred to as the “Mancos B.” This sandy unit forms conspicuous, tan-colored, low, dendritically incised hills and ridges in the map area. The unit top, about 4 m below the Kmu contact, contains two horizons that contain large (1 to 2 m) septarian dolomite concretions that contain clear to translucent calcite and locally includes bluish- to cola-colored barite crystals. These concretions are sought by mineral collectors in the Grand Valley. Basal contact with the Smoky Hill Member (Kms) is marked by: the lack of interlaminated sandstone; darker gray color change; the presence of calcareous shale and light-gray shaly limestone beds; and general subdued topography. Unit Kmp is about 306 m thick (Cole and others, 1997). | 02.02 | DMUUnit1 | Kmp | Kmp | 211-255-190 | None | DAS1 | Sandstone and mudstone | High | DMU29 |
| 28 | Kms | Smoky Hill Member (lower Blue Gate Member) | Smoky Hill Member (lower Blue Gate Member) | Upper Cretaceous | Dark gray to gray-black, finely fissile, speckled, moderately to very calcareous, poorly indurated shale; light-gray, platy to sub-blocky, poorly-to-moderately indurated, shaly limestone; and a lower interval composed of interlaminated, moderately cemented, very fine to fine-grained sandstone. Unit contains sporadic thin (≤ 6 cm) bentonite beds. Specks are predominantly coccoliths and may be concentrated along bedding planes to locally form light-gray interlaminations (~1 mm). Thick-shelled, prismatic | 02.03 | DMUUnit1 | Kms | Kms | 125-196-64 | None | DAS1 | Mostly mudstone | High | DMU30 |
| 29 | Kml | Lower part of the Mancos Shale | Lower part of the Mancos Shale (Ferron Sandstone and Tunuck Member) | Upper Cretaceous | Includes the Montezuma and Juana Lopez members (Ferron Sandstone Member), and the Blue Hill, Coon Springs Sandstone, Bridge Creek Limestone, and Graneros members (Tunuck Member) (White and others, 2015). Shown in cross section only. | 02.04 | DMUUnit1 | Kml | Kml | 178-204-46 | None | DAS1 | Mostly mudstone | High | DMU31 |
| 30 | Kdb | Dakota Sandstone and Burro Canyon Formation, undivided | Dakota Sandstone and Burro Canyon Formation, undivided | Lower Cretaceous | Shown in cross section only. | 02.05 | DMUUnit1 | Kdb | Kdb | 178-178-102 | None | DAS1 | Mostly sandstone | High | DMU32 |
| 35 | Jm | Morrison Formation | Morrison Formation | Upper Jurassic | Includes the following members: Brushy Basin mudstone and sandstone, the Salt Wash sandstone, and the Tidwell mudstone, sandstone, and limestone (Scott and others, 2001; White and others, 2015). Shown in cross section only. | 02.06 | DMUUnit1 | Jm | Jm | 204-255-230 | None | DAS1 | Mostly mudstone | High | DMU33 |
| 31 | Mz | Formations of the Middle Jurassic to Upper Triassic age, undivided | Formations of the Middle Jurassic to Upper Triassic age, undivided | Mesozoic | Includes the Wanakah Formation, Entrada Sandstone, Kayenta Formation, Wingate Sandstone, and Chinle Formation (Scott and others, 2001; White and others, 2015). Shown in cross section only. | 02.07 | DMUUnit1 | Mz | Mz | 168-243-234 | None | DAS1 | Clastic sedimentary rock | High | DMU34 |
| 32 | Xu | Precambrian rock of the Uncompahgre Uplift, undivided | Precambrian rock of the Uncompahgre Uplift, undivided | Paleoproterozoic | Gneiss and migmatite (Scott and others, 2001). Shown in cross section only. | 02.08 | DMUUnit1 | Xu | Xu | 179-153-153 | None | DAS1 | Igneous and metamorphic rock | None | DMU35 |
| 33 | water | water | water | Holocene | None | 03.01 | DMUUnit1 | water | water | 190-232-255 outline 0-132-168 | None | DAS1 | Water or ice | High | DMU36 |
| OBJECTID | Term | Definition | DefinitionSourceID | Glossary_ID |
|---|---|---|---|---|
| 35 | 1 SD | A statistic used as a measure of the dispersion or variation in a distribution or set of data, equal to the square root of the arithmetic mean of the squares of the deviations from the arithmetic mean. | DICT1 | GLO01 |
| 12 | Age | the length of time during which a being or thing has existed; length of life or existence to the time spoken of or referred to | DICT1 | GLO02 |
| 3 | anticline | A fold in rock strata with a convex upward shape. The rocks in the core of an anticline are the oldest. Identity and existence certain, location accurate | GEODICT1 | GLO03 |
| 16 | Bedding | In this context, bedding refers to a measurement convention used to describe the orientation, or attitude, of a planar geologic feature. A feature's strike is the azimuth of an imagined horizontal line across the plane, and its dip is the angle of inclination measured downward from horizontal. | GEODICT1 | GLO04 |
| 17 | Bedding1 | In this context, bedding refers to a measurement convention used to describe the orientation, or attitude, of a planar geologic feature. A feature's strike is the azimuth of an imagined horizontal line across the plane, and its dip is the angle of inclination measured downward from horizontal. In this context, these strike and dips were estimated from LiDAR data. | GEODICT1 | GLO05 |
| 33 | Bedding2 | In this context, bedding refers to a measurement convention used to describe the orientation, or attitude, of a planar geologic feature. A feature's strike is the azimuth of an imagined horizontal line across the plane, and its dip is the angle of inclination measured downward from horizontal. In this context, these strike and dips were estimated from LiDAR data. | GEODICT1 | GLO06 |
| 20 | borrow pit | A pit created to provide earth that can be used as fill at another site | DICT1 | GLO07 |
| 6 | boundary | A line that marks the limits of an area | DICT1 | GLO08 |
| 1 | certain | Identity of a feature can be determined using relevant observations and scientific judgment; therefore, one can be reasonably confident in the credibility of this interpretation. | FGDC-STD-013-2006 | GLO09 |
| 5 | contact | A geological contact is a boundary which separates one rock body from another. A contact can be formed during deposition, by the intrusion of magma, or through faulting or other deformation of rock beds that brings distinct rock bodies into contact. | GEODICT1 | GLO11 |
| 15 | Cross Section | A graphic representation of the intersection of the geological bodies in the subsurface with a vertical plane of a certain orientation showing relationships between rock units | GEODICT1 | GLO12 |
| 11 | Deposit type | Groupings for surficial units in the CMU | DAS1 | GLO13 |
| 34 | DH Trace | The down hole course created by drilling into the subsurface | DICT1 | GLO14 |
| 8 | DMUHeading1 | GeMS hierarchy formatting term | GeMS1 | GLO15 |
| 9 | DMUHeading2 | GeMS hierarchy formatting term | GeMS1 | GLO16 |
| 10 | DMUUnit1 | GeMS hierarchy formatting term | GeMS1 | GLO17 |
| 29 | Elev | The vertical distance between a standard reference point, such as sea level, and the top of an object or point on the Earth | DICT1 | GLO19 |
| 7 | fault | A fault is a fracture or zone of fractures between two blocks of rock. Faults allow the blocks to move relative to each other; a planar surface of rupture along which geologic units have been fractured and then displaced. | GEODICT1 | GLO20 |
| 36 | Feature | a prominent or conspicuous part or characteristic | DICT1 | GLO21 |
| 27 | FltMvmt1 | Cartographic symbols showing the relative offset on the fault in cross section | DAS1 | GLO22 |
| 28 | FltMvmt2 | Cartographic symbols showing the relative offset on the fault in cross section | DAS1 | GLO23 |
| 18 | gravel pit | A gravel pit is an open-pit mine for the extraction of gravel. | GEODICT1 | GLO24 |
| 32 | gypsum deposit | An accumulation of a widely distributed mineral consisting of aquated calcium sulfate: CaSO4•2H2O . It is the commonest sulfate mineral, and is frequently associated with halite and anhydrite in evaporites, forming thick, extensive beds interstratified with limestone, shale, and clay (esp. in rocks of Permian and Triassic age). Gypsum is soft (hardness of 2 on the Mohs scale); it is white or colorless when pure, but commonly has tints of gray, red, yellow, blue, or brown. It occurs massive (alabaster), fibrous (satin spar), or in monoclinic crystals (selenite) Gypsum is used chiefly as a soil amendment, as a retarder in portland cement, and in making Plaster of Paris. Etymol: Greek "gypsos", "chalk". Syn: gypsite; gyp; plaster stone. | GEODICT1 | GLO25 |
| 37 | High | unusual or considerable in degree, power, intensity, etc. | DICT1 | GLO34 |
| 30 | O&G well | An oil well is a boring in the Earth that is designed to bring petroleum oil hydrocarbons to the surface. Usually some natural gas is released as associated petroleum gas along with the oil. A well that is designed to produce only gas may be termed a gas well. | GEODICT1 | GLO26 |
| 19 | OSL sample site | Optically-Stimulated Luminescence is a late Quaternary dating technique used to date the last time quartz sediment was exposed to light. As sediment is transported by wind, water, or ice, it is exposed to sunlight and zeroed of any previous luminescence signal. | DAS1 | GLO27 |
| 2 | questionable | Identity of a feature cannot be determined using relevant observations and scientific judgment; therefore, one cannot be reasonably confident in the credibility of this interpretation. For example, IdentityConfidence = questionable is appropriate when a geologist reasons "I can see some kind of planar feature that separates map units in this outcrop, but I cannot be certain if it is a contact or a fault." | FGDC-STD-013-2006 | GLO28 |
| 22 | surface | The topographic profile of the cross section | DAS1 | GLO29 |
| 4 | syncline | A trough-shaped fold with youngest strata in the center | GEODICT1 | GLO30 |
| 21 | water | a colorless, transparent, odorless liquid that forms the seas, lakes, rivers, and rain and is the basis of the fluids of living organisms. | GEODICT1 | GLO31 |
| 31 | Water well | Wells (bore holes) that penetrate artesian aquifers. Water will rise up the well casing to the pressure level of the aquifer. Artesian flow describes the natural flow to the surface of water from confined aquifers. | GEODICT1 | GLO32 |
| 26 | yr | the time taken by the earth to make one revolution around the sun | DICT1 | GLO33 |
| OBJECTID | MapProperty | MapPropertyValue | MiscellaneousMapInformation_ID |
|---|---|---|---|
| 1 | PHYSIOGRAPHIC SETTING | The Badger Wash quadrangle lies in Mesa and Garfield Counties, Colorado, approximately 24 km northwest of the town of Fruita and 4.4 km east of the Utah border. The quadrangle lies at the northwestern edge of the Grand Valley where agricultural lands are irrigated by the Government Highline Canal. The Grand Valley is a topographically low area of subdued hills and badlands that lie between the Uncompahgre Plateau and the Book Cliffs. Access to the quadrangle map area is best from Old Highway 6&50 to Garfield County Road 201 (Baxter Pass Road) that follows the West Salt Creek valley into the Book Cliffs. The topography in the southern part of the map area consists of wide and subdued flats, low hills, and low (<50-m high) mesas, The small mesas are capped with Pleistocene alluvial-fan and stream terrace gravel, which are now topographically inverted. North of the flat irrigated lands and the canal in the map area, the underlying Mancos Shale bedrock is more sandy and more resistant to weathering and erosion. Shallow dendritic drainage patterns are developed in low hills and ridgelines that rise from 70 to 90 m above the irrigated lands. The major creeks are intermittent or ephemeral. They included Badger Wash and Prairie Canyon creeks that are tributaries of West Salt Creek. The confluence of West Salt and East Salt creeks occurs 1.7 km below the southern map boundary where the Salt Creek thalweg extends an additional 5 km to its confluence with the Colorado River in Ruby Canyon. The highest elevation of the Badger Wash quadrangle is 1,632.5 m above mean sea level (AMSL) at the north-central map boundary on a high narrow mesa capped by rocky and resistant Pleistocene alluvial-fan deposits. The lowest elevation is 1,376.3 m AMSL at the southern map boundary where East Salt Creek flows though the southeastern corner of the map area. The climate is arid and vegetation outside of irrigated areas is sparse. The landscape is comprised in part of adobe-type badlands that are common in the Colorado (Grand), Gunnison, and the Uncompahgre River valleys of west-central Colorado where the Mancos Shale bedrock is exposed. The annual precipitation ranges from 20 to 30 cm (National Centers for Environmental Information). | MMI01 |
| 2 | GEOLOGIC SETTING | The oldest bedrock unit exposed in the map area is the Late Cretaceous Mancos Shale. The marine shale was deposited during the transgression of the Cretaceous Western Interior Seaway (WIS) (Franczyk and others, 1992). Regressive and transgressive sequences of the western shoreline of the WIS formed the sediments of the Iles and Williams Fork formations of the Mesa Verde Group. These rocks are more resistant to weathering and form the Book Cliffs that are exposed north of the map area. Off map to the south, faulting and monoclinal folding of the northeast front of the Uncompahgre Uplift exposes earlier Mesozoic rocks and Proterozoic basement rocks of the Uncompahgre Plateau in the Colorado National Monument (Scott and others, 2001) and the McInnis Canyons National Conservation Area south of the Colorado River (White and others, 2015). The exposed package of Triassic and Jurassic sedimentary rocks includes the basal Triassic Chinle Formation, which nonconformably overlies Proterozoic basement rocks. This type of unconformity indicates an earlier Pennsylvanian-Permian uplift of the Ancestral Uncompahgre Mountains. Earlier Paleozoic sedimentary rocks that were exposed in the ancestral uplift were subsequently eroded away over millions of years. The Triassic Period ground surface in the Mesozoic Era was beveled to a peneplain eroded down to crystalline Proterozoic basement rocks prior to the deposition of later Mesozoic and Cenozoic sedimentary rocks. These rocks were later uplifted during the Laramide Orogeny when the faulting and folding of the Uncompahgre uplift occurred and formed the present-day Uncompahgre Plateau. The Grand Valley was formed by Late Neogene to Pleistocene erosion and long-term ground lowering by the Colorado River and its tributaries where the less resistant Mancos Shale was at ground surface (Aslan and others, 2019). The structural geology of the Badger Wash quadrangle reflects the regional faulting along the general northwest to southeast trend of the Uncompahgre Uplift. The general dip of the strata is north to northeast towards the Unita and Piceance basins. Structural data were difficult to obtain because of the weathering of the exposed shale bedrock. However, useful attitudes of the bedrock were gained from exposures of tabular sandy dolomite concretionary beds, very thin beds of bentonite, and thinly interbedded sandstone beds of the Prairie Canyon Member. The major structural features in the map area are several subparallel normal faults, shallow folds, and the termination of the Flume Creek monoclinal fold that is expressed in the dip of Mancos Shale near the southwest corner of the quadrangle near Old Highway 6&50. This monocline trend extends northwest from the Mack area and is likely fault cored at depth (White and others, 2015). Field work for this study identified surface faulting, shallow-displacement grabens, and paired anticlines and synclines. These southwest to northeast trending subparallel branch faults were first mapped by Krey (1962). These faults are also shown in the 1:250,000-scale (Cashion, 1973) and 1:100,000-scale (Ellis and Gabaldo, 1989) geologic maps. However, several other subparallel normal faults were identified during the mapping of the Badger Wash quadrangle. Significant structural variation was also noted in exposed bedrock strata within the faulted terrain, as well as localized deformation of strata near faults. Crystalline calcite filling that locally include casts of fault and shear zone slickensides were also observed. The faults trend approximately 70 to 80 degrees (north to northeast) from the general southeast to northwest trend of the folded front of the Uncompahgre Uplift at the Flume Creek monocline. | MMI02 |
| 3 | WATER RESOURCES | Water resources of the Badger Wash are minimal. The Underlying Mancos Shale members are not water bearing and the water quality of older Mesozoic rocks at depth is poor. Streams only flow intermittently during high precipitation events. The cobble-rich alluvial aquifer composed of lower Colorado River terraces gravels of the Grand Valley is not present in the map area. This buried water bearing cobbly deposit ends where the Colorado River has incised into Horsethief Canyon between Fruita and Mack (Butler and others, 1996). Government Highline Canal provides water to irrigate farmlands in the lower third of the quadrangle. Canal water empties into West Salt Creek, which marks the western end of irrigated farmlands in the Grand Valley of Colorado. | MMI03 |
| 4 | MINERAL RESOURCES | Oil and Gas resources are present in the quadrangle (Colorado Energy and Carbon Management Commission (ECMC)). Named oil and gas fields include portions of the Bar-X, Bidle, and Peachtree fields (ECMC). These fields were developed in the structural terrain mentioned above (Krey, 1962). For most of the oil and gas wells, the total depth was in the Entrada Sandstone and production predominantly occurred from the Dakota Sandstone and Burro Canyon Formation (Kdb) and the Entrada Sandstone (Je). These units are not exposed in the map area but are shown in the cross section. Within the Mancos Shale, the Niobrara Member may have oil and gas potential using horizontal well drilling and hydraulic fracturing (fracking) completion techniques. There are small gravel pits in some of the mesa surfaces underlain by old gravels, but the quality is poor, being low-durability sandstone-rich gravel derived chiefly from Mesa Verde Group rocks of the Book Cliffs and locally containing channels or layers composed of mud-flow and debris-flow deposits with a clay matrix. | MMI04 |
| 5 | GEOLOGIC HAZARDS | Potential geologic hazards in the map area are primarily the risks posed by stream flooding as well as mudflow and debris flow deposition. The floors of the intermittent stream show evidence of flooding, scour, and deposition of bouldery gravel. The Mancos Shale contains bentonite and other expansive clay minerals. Clayey surficial deposits (soils in geotechnical engineering terms) derived from the shale may be expansive (swelling soils). Some silty to clayey sand deposits may also be low density and may be collapsible and settle upon wetting (hydrocompactive soils). Unimproved dirt road and 4WD tracks in the adobe badlands may become impassable when they are wet as the clay soils becomes increasingly slick, greasy, and adhere to tires and shoes. The marine shale may also be high in sulfates and may be corrosive to unprotected concrete and steel. High selenium levels and other dissolved solids have been reported in irrigation return waters in the Mancos Shale (Butler and other, 1996). Site-specific geotechnical investigations including bore holes and soil testing should be conducted for structures planned in the Mancos Shale or in clayey soils derived from the Mancos. | MMI05 |
| 6 | PREVIOUS GEOLOGIC MAPPING | The preparation of this map was aided by the review of previous geologic mapping conducted in the area. The geology of the Badger Wash quadrangle was previously mapped at 1:100,000 scale by Ellis and Gabaldo (1989) and at the 1:250,000 scale (1° by 2°) by Cashion (1973). Krey (1962) prepared a small-scale structural map of the area. On an adjacent 1:24,000-scale quadrangle at the southeast corner of the Badger Wash quadrangle, the geology of the Mack quadrangle was mapped by White and others (2015) as part of this multi-year mapping program in the Grand Valley by the Colorado Geological Survey. The 1:24,000-scale quadrangle adjacent to the Badger Wash quadrangle are shown in the index map on Plate 1. | MMI06 |
| 7 | ACKNOWLEDGMENTS | The bulk of the property of the Badger Wash quadrangle is federal lands administered by the U.S. Bureau of Land Management. High-resolution orthorectified aerial photography and tax assessor land parcel data was downloaded from the Mesa County GIS Department web site. Pangaea Geospatial produced the map plates and GIS files for this publication. This map publication benefited from reviews by Ralph Shroba and Matthew Morgan of the Colorado Geological Survey. | MMI07 |
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Wintle, A.G. and Murray, A.S., 2006, A review of quartz optically stimulated luminescence characteristics and their relevance in single-aliquot regeneration dating protocols: Radiation Measurement, v. 41, p. 369-391. | MMI08 |
| 9 | TITLE | GEOLOGIC MAP OF THE BADGER WASH QUADRANGLE, MESA AND GARFIELD COUNTIES, COLORADO | MMI09 |
| 10 | AUTHOR | Jonathan L. White and Emily A. Perman | MMI10 |
| 11 | YEAR | 2024 | MMI11 |
| 12 | STATEMAP AGREEMENT | This mapping project was funded jointly by the Colorado Geological Survey and the U.S. Geological Survey through the National Cooperative Geologic Mapping Program under STATEMAP agreement G22AC00302. | MMI12 |