GeMS validation of OF-21-03_DryCreek.gdb

File written by GeMS_ValidateDatabase.py, version of 3/28/2024
Mon Jul 29 08:24:41 2024
Runtime parameters
Database path: C:\Data\Pangaea\CGS\_2024 Submitted Projects\2021 Dry Creek\OF-21-03_DryCreek\OF-21-03_DryCreek_Publication\OF-21-03_DryCreek_Database\OF-21-03_DryCreek.gdb
Output directory: C:\Data\Pangaea\CGS\_2024 Submitted Projects\2021 Dry Creek\validation
Metadata file: C:\Data\Pangaea\CGS\_2024 Submitted Projects\2021 Dry Creek\OF-21-03_DryCreek\OF-21-03_DryCreek_Publication\OF-21-03_DryCreek_Metadata.xml
Check embedded metadata: False
Skip topology check: False
Refresh GeoMaterialDict: True
Delete extra rows in Glossary and DataSources: False
Compact GDB: True

This database is LEVEL 3 COMPLIANT.

The database-level FGDC metadata are formally correct although the metadata record should be reviewed to verify that it is meaningful.

This file should be accompanied by OF-21-03_DryCreek.gdb-ValidationErrors.html and OF-21-03_DryCreek_Metadata.xml_errors.txt in the same directory.

If this database will be submitted to the NGMDB, it also needs to be accompanied by a reviewed Geologic Names report that includes identification of any suggested modifications to Geolex. Use the Geologic Names Check tool to generate that report or provide other documentation of a review.

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Contents

Compliance Criteria
Warnings
Content not specified in GeMS schema
Occurrence of MapUnits in DMU, feature datasets, or geopackage tables
Contents of Nonspatial Tables
DataSources
DescriptionOfMapUnits
Glossary
MiscellaneousMapInformation
Database Inventory

Compliance Criteria

LEVEL 1

Criteria for a LEVEL 1 GeMS database are: Databases with a variety of schema may meet these criteria. This script cannot confirm LEVEL 1 compliance.

LEVEL 2--MINIMALLY COMPLIANT

A LEVEL 2 GeMS database is accompanied by a peer-reviewed Geologic Names report, including identification of suggested modifications to Geolex, and meets the following criteria:
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

LEVEL 3--FULLY COMPLIANT

A LEVEL 3 GeMS database meets these additional criteria:
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

Warnings

There are 13 warnings

Content not specified in GeMS schema

Some of the extensions to the GeMS schema identified here may be necessary to capture geologic content and are entirely appropriate. Please document these extensions in metadata for the database, any accompanying README file, and (if applicable) any transmittal letter that accompanies the dataset. Other extensions may be intermediate datasets, fields, or files that should be deleted before distribution of the database.

Fields


Tables


CorrelationOfMapUnits
CrossSectionA
GenericPoints
CoalBoringAnno
ContactsAndFaultsAnno
MapUnitPolysAnno
MineSitesAnno
OandGWellAnno
OrientPointsAnno
WaterWellAnno
DepositAnno
AgeAnno
MapPolyAnno
CSACartoLines
CSACartoLinesAnno
CSAMapUnitPolysAnno

Occurrence of MapUnit in DMU, feature datasets, or geopackage tables

MapUnit DescriptionOfMapUnits CrossSectionA GeologicMap CorrelationOfMapUnits
Qco X -- X X
Qa X -- X X
water X -- X --
Qg1 X -- X X
Qdf X -- X X
Km X X -- X
PEw X X X X
Kicz X X X X
Mz X X -- --
Qg8 X -- X X
Qg6 X -- X X
Qc X -- X X
Qg3 X X X X
Qg7 X X X X
Kdb X X -- --
pC X X -- --
PEg X X X X
QNg10 X -- X X
Qg5 X -- X X
Qlso X -- X X
Kir X X X X
Qg2 X -- X X
Qaf X X X X
Qlsi X X X X
Qac X -- X X
Kw X X X X
Kmu X -- X X
Qefr X -- X X
Qlsu X X X X
Qefi X -- X X
af X -- X X
Qg4 X X X X
Qlsr X -- X X

Contents of Nonspatial Tables

DataSources

OBJECTIDSourceNotesURLDataSources_ID
8American Geosciences Institute online gossary of geologyNonehttps://glossary.americangeosciences.org/AGI1
3DAS1NoneThis studyDAS1
9Online dictionaryNonewww.dictionary,.comDICT1
4Colorado Division of Water ResourcesNonehttps://dwr.colorado.gov/DWR
6Colorado Energy and Carbon Management CommissionNonehttps://ecmc.state.co.usECMC
1Federal 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.Nonehttps://ngmdb.usgs.gov/fgdc_gds/geolsymstd.phpFGDC-STD-013-2006
7GeMS standardNonehttps://pubs.usgs.gov/publication/tm11B10GEMS1
5US Geological SurveyNonehttps://www.usgs.gov/USGS

DescriptionOfMapUnits

OBJECTIDMapUnitNameFullNameAgeDescriptionHierarchyKeyParagraphStyleLabelSymbolAreaFillRGBAreaFillPatternDescriptionDescriptionSourceIDGeoMaterialGeoMaterialConfidenceDescriptionOfMapUnits_ID
1NoneSURFICIAL DEPOSITSSURFICIAL DEPOSITSNoneMaps units are described using the following classifications: grain sizes chart modified from Wentworth (1922); bedding thickness terms codified in the current classification of the Society for Sedimentary Geology (SEPM); and degree of calcareousness in rock and soils judged by intensity of effervescence (fizz or bubbling in a liquid) that resulted from the introduction of 10% hydrochloric acid (HCl) to a rock or soil sample in the field. Development stages of calcic soils are from Machette (1985).01DMUHeading1NoneNoneNoneNoneDAS1NoneNoneDMU01
2NoneHUMAN-MADE DEPOSITSHUMAN-MADE DEPOSITSNoneNone01-01DMUHeading2NoneNoneNoneNoneDAS1NoneNoneDMU02
3afArtificial fillArtificial filluppermost HoloceneGravel, sand, silt, and clay emplaced by human activities, predominantly for road embankments and reservoir dams. Unit may include controlled engineered fill, uncontrolled unsorted rocky fill, and locally disturbed ground. Thickness is variable, with embankment fills measured up to 15 m thick.01-01-01DMUUnit1afaf255-255-255NoneDAS1"Made" or human-engineered landHighDMU03
4NoneALLUVIAL DEPOSITSALLUVIAL DEPOSITSNoneNone01-02DMUHeading2NoneNoneNoneNoneDAS1NoneHighDMU04
5QaAlluvial depositsAlluvial depositsUpper HoloceneTan-gray, poorly sorted, boulder to pebbly gravel, sand, silt, and clay that are typically deposited by seasonal flash floods. Clasts are typically subangular to rounded Neogene basaltic rocks of the Grand Mesa Volcanic Field (GMVF) (Cole and others, 2017), reworked from alluvial (Qg) and landslide deposits. In some locations, sandstone clasts are present in the unit where streams flow near exposures of Williams Fork Formation (Kw) and Rollins Sandstone (Kir). Deposits typically occur along the floors of incised creek channels. The unit is typically not mapped if the channel is narrow (<12 m wide). Finer-grained gravelly mud Qa sediments also locally occur in meanders that have been incised into valley-fill deposits (Qaf). Thicknesses are variable. In some locations, unit is limited to bed-load sediments in ravines, but in broader channels likely does not exceed 1.5 to 2 m in thickness. Areas of unit Qa along narrow creek bottoms, ravines, and channels are periodically subject to dangerous flash flooding events.01-02-01DMUUnit1QaQa255-255-115NoneDAS1Alluvial sediment, mostly coarse-grainedNoneDMU05
6QafAlluvium and alluvial-fan depositsAlluvium and alluvial-fan depositsHolocene to Upper PleistoceneGray to dark-brown to dark reddish-brown, unsorted to poorly sorted, poorly to moderately stratified, sandy to silty clay that locally may contain gravelly lenses and dispersed pebble- to boulder-sized clasts. The unit contains valley-fill deposits of coalesced alluvial fans and may include unmapped alluvial-colluvial (Qac) sediments including slopewash, and mudflows transported from local soil-slip landslides on adjacent hillsides. The typical deposit generally consists of fine-grained sediments transported as sandy mud derived from clay-rich bedrock onto gentle to moderately sloping valley sides and where valley floors widen when underlain by the upper part of the Mancos Shale (Kmu). The unit locally may contain shale and sandstone fragments and can be gravelly with reworked basaltic pebble- to cobble-sized clasts eroded from older and higher landslide deposits (Qlsu) and gravel (Qg) units within the drainage basin. The unit locally may be incised by younger stream alluvium (Qa) in valleys such as Currant and Dry creeks. Unit Qaf is also mapped in broad swales and shallow valleys on the lower flanks of mesa risers, near exposed bedrock, and low-gradient landslide terrain such as slump-block depressions where the unit is more typical of slopewash. Unit thickness is variable but in water-well logs ranges from 6 to 43 m near where an unnamed stream outlets (T13S, R93W, Sec. 22) onto the broadened valley of coalesced alluvial fans above the confluence of Dever Creek to Leroux Creek. In slopewash swales, unit is likely to be thinner. Flash flooding and mud and (or) debris flows locally may occur in and downstream of the many tributary channels that discharge onto and through this unit. In areas where unit Qaf sediments are derived from expansive clay minerals such as in the Mancos Shale, swelling-soil hazards may locally occur.01-02-02DMUUnit1QafQaf255-235-175190-210-255; 502 periglacialDAS1Alluvial sediment, mostly fine-grainedNoneDMU06
7NoneMixed Alluvial and Debris-Flow Gravel DepositsMixed Alluvial and Debris-Flow Gravel DepositsNoneBasaltic gravel deposits at various heights above stream level and of different ages cover extensive areas throughout the map area where they aggraded and formed broad treads of coalesced glacio-fluvial outwash, debris-flow fans, and paleovalley-fill sediments. Through the process of topographic inversion, these deposits now form a series of elevated and dissected, gravel-capped, relatively flat-lying treads along Surface, Currant, and Leroux creeks. The gravel deposits remnants are typically older at progressively higher elevations above the current creek level and where they have alluvial fan-like geometries with surface profiles that slope upward toward sediment source areas high on the southern flank of Grand Mesa. Old landslides (Qlso) typically mantle the flanks of the high mesa. Assigning relative age to the older gravel deposits is complex; the segregation and isolation of alluvial-fan deposition had been separated by paleo-bedrock drainage divides that have been long removed by later Pleistocene erosion, which may locally result in both differing elevations and longitudinal slope profiles of the high mesas. In all Qg units, three major types of deposits are locally present: 1) tan to tan-gray, debris-flow deposits, stratified by individual flow events, containing very poorly sorted, sub-angular pebbles to boulders in an unsorted sandy-mud matrix that contain very large boulder (< 2.5 m) trains and levees; 2) gray, riverine, alluvial deposits containing beds of sub-rounded to well-rounded pebbles to small boulders, densely packed and imbricated in a moderate- to well-sorted sand matrix; and 3) olive-gray to tan-gray, fine-grained, thinly bedded to interlaminated sandy mudflow deposits with scattered, matrix-supported pebbles to small boulders. Cut-and-fill channel deposits are typically composed of debris-flow deposits. Gravel clasts in the deposit are composed chiefly of basaltic rocks of the GMVF. Minor amounts (<5% are non-basaltic rock types) of sandstone, siltstone, clinker, chert, carbonate concretions, and well-rounded polylithic pebbles and cobbles are locally present. These minor clasts are eroded from Upper Cretaceous rocks or reworked from Paleogene- to Miocene-aged sedimentary rock within the drainage basin. The thickness of the deposits varies within individually mapped gravel units listed below. The degree of weathering and calcic soil development (Bk horizon) increases with the increasing age of the deposits. Topsoil on the older units is typically reddish-brown to reddish-tan, and significant erosion and weathering of the ground surfaces has occurred. The reddish-brown topsoil has a pinkish-white chalky appearance in many areas because of the erosion of surface soil horizons and exposure of the well-developed Bk calcic soil horizon. This horizon is best exposed along mesa rims. Basaltic boulders, exposed to long-term surface weathering, are heavily stained, fractured, and have weathering pits. With increasing age, sediments are typically more consolidated, and streaks of blue-gray mineral staining are locally common. Locally the basal zones of some of the older deposits have sufficient calcite cement to form conglomerate that outcrop as subtle ledges at the base of the deposits. Side slopes and swales eroded into risers of the older units are typically mantled with deposits of unit Qaf, old colluvial deposits (Qco), and landslide deposits. Terminology for gravel deposits generally follows Noe and Zawaski (2013) and Noe and others (2015a and 2015b). However, at the southern map boundary, this map area differs in the enumeration of Late Pleistocene units. Gravel deposits are present at ten levels in the map area. Point symbols on gravel deposits indicate thicknesses of basaltic gravel taken from water-well log data accessed from the Colorado Division of Water Resources (DWR) map viewer.01-03DMUHeading2NoneNoneNoneNoneDAS1NoneNoneDMU07
8Qg1Gravel deposit oneGravel deposit oneLower HoloceneUnit underlies lowest terrace level on valley floors. The unit surface is typically 6 to 9 m above the current stream level channel that contains unit Qa. Unit is poorly exposed and typically buried by valley-fill (Qaf) deposits. 01-03-01DMUUnit1Qg1Qg1255-255-21585-255-0; 605 breccia openDAS1Alluvial sediment, mostly coarse-grainedHighDMU08
9Qg2Gravel deposit twoGravel deposit twoLower Holocene to Upper PleistoceneQg2 deposits underlie terrace tread remnants that mainly occur along Currant Creek about 20 m above stream level. Water-well logs penetrated 6 to 16 m of Qg2 basaltic gravel overlying shale bedrock (Kmu). 01-03-02DMUUnit1Qg2Qg2255-255-215255-127-127; 605 breccia openDAS1Alluvial sediment, mostly coarse-grainedHighDMU09
10Qg3Gravel deposit threeGravel deposit threeUpper PleistoceneUnit Qg3 includes extensive terrace treads of the major creeks (Surface, Currant, and Leroux creeks) in the map area. These creeks have extensive drainage basins that extend northward of the map, into Grand Mesa highlands. The unit has a moderately developed, Calcic Stage II, Bk horizon and the topsoil has a reddish-tan to reddish-brown color. Where exposed, clasts are heavily encrusted with chalky-white colored CaCO3. This unit yielded an optically stimulated luminescence (OSL) age estimate of 19,245±1,640 yrs BP within the adjacent Cedaredge quad (White, 2023). The total thickness of the unit varies: water-well borings exceeded 100 m in basaltic gravel along Surface Creek; Leroux Creek terrace treads range from 26 m to 69 m thick, but many water wells with total depths exceeding 50 m terminate in basaltic gravel; and thinner Currant Creek treads range from 5 and 20 m thick. The surface of this deposit above modern stream elevation ranges from 25 to 32 m, except for Leroux Creek at the southern border of the map area, where stream incision into Mancos Shale has increased the height of the Qg3 surface to about 55 m above the modern stream level. The gravel that underlies this surface were likely deposited as glacio-fluvial outwash during the Pinedale glaciation (Marine Isotope Stage 2 (MIS 2)) on Grand Mesa north of the map area. 01-03-03DMUUnit1Qg3Qg3255-255-215115-161-230; 605 breccia openDAS1Alluvial sediment, mostly coarse-grainedHighDMU10
11Qg4Gravel deposit fourGravel deposit fourUpper PleistoceneDeposits of unit Qg4 underlie terrace remnants and treads along Currant Creek above the confluence with Dry Creek. A sample collected from this unit within the adjacent Cedaredge quad yielded an OSL age estimate of 34,145±2,560 yrs BP (White, 2023). The topsoil of this unit has a reddish-brown color and a well-developed, stage III+, calcrete K soil horizon is present where exposed at a landslide scarp. Water-well logs and measurements at the landslide scarp exposure reveal a thickness of about 11 m. The terrace surface elevation is 38 to 55 m above the modern stream level. Deposits of unit Qg4 may correlate to the early Pinedale glaciation (MIS 3) (Sturchio and others, 1994).01-03-04DMUUnit1Qg4Qg4255-255-215230-0-169; 605 breccia openDAS1Alluvial sediment, mostly coarse-grainedHighDMU11
12Qg5Gravel deposit fiveGravel deposit fiveupper Middle PleistoceneThe Qg5 unit underlies one local mesa remnant in the map area above the confluence of Currant and Dry creeks. No water-well data is available, but the thickness of the unit is estimated to be less than 5 m. The surface of this remnant is 75 m above the current level of Currant Creek. Deposits of unit Qg5 may correlate with the outwash of the Bull Lake glaciation (MIS 6).01-03-05DMUUnit1Qg5Qg5255-255-215255-170-0; 605 breccia openDAS1Alluvial sediment, mostly coarse-grainedHighDMU12
13Qg6Gravel deposit sixGravel deposit sixupper Middle PleistoceneGravel remnants of unit Qg6 form a long (4.4 km) curving tread deposited on the eastern flank of the Cedar Mesa gravel deposit (Qg7). The deposit surface is 120 m above stream base level at Cactus Park, but only 57 m above the modern stream level at the confluence of Currant and Dry creeks. The topsoil is a reddish-brown color, and the deposit has developed a strong K soil horizon (calcic Stage IV+). Water wells on the Qg6 deposit penetrated 20 m of basaltic gravel. In a recent road excavation for Cedar Mesa Road, the 20 m-thick riverine gravel filled a gullied paleosurface in the Mancos Shale (Kmu). Based on height above current stream levels, soil development, and elevation relationship with other gravel units, Qg6 unit may correlate with an early phase Bull Lake glaciation (MIS 6).01-03-06DMUUnit1Qg6Qg6255-255-2150-168-132; 605 breccia openDAS1Alluvial sediment, mostly coarse-grainedHighDMU13
14Qg7Gravel deposit sevenGravel deposit sevenlower Middle PleistoceneUnit Qg7 forms an ancient, massive, and prominently high-elevation alluvial fan named Cedar Mesa near the southwest corner of the map area. The center of the mesa is about 120 m above the present stream level of the confluence of Currant and Dry creeks. The topsoil is silty clay, reddish-brown in color, and contains reworked loess at the surface. Below the reddish-brown topsoil is a ~1-m thick, well-developed Km horizon (calcic Stage IV) that forms a chalky-white-colored band in the deposit exposed at landslide scarps. Near and above the mesa rims, the strong K horizon also forms a pinkish-white, well-consolidated calcrete that weathers into abundant angular pebble-sized clasts in a chalky-white matrix. Unit thickness is variable and likely reflects the aggradation of a gravel fan in a topographic low such as a preexisting valley. Water wells penetrated between 32 to 59 m of basaltic bouldery gravel before hitting Mancos Shale (Kmu). The unit is at a higher elevation than Petrie Mesa in the North Delta quadrangle, where Noe and others (2015a) reported the presence of Lava Creek B ash (631 ka, Matthews and others, 2015). However, it is not clear whether the mesa elevations correspond to the same approximate age. The author did not observe the ash in the map area or in the Cedaredge quadrangle (White, 2023).01-03-07DMUUnit1Qg7Qg7254-251-221132-0-168; 605 breccia openDAS1Alluvial sediment, mostly coarse-grainedHighDMU14
15Qg8Gravel deposit eightGravel deposit eightLower PleistoceneUnit Qg8 gravel forms a massive alluvial fan called Redlands Mesa that extends southward beyond the map area. This older bouldery gravel deposit has reddish-brown topsoil (hence its name), a discontinuous mantle of reworked reddish-brown loess, and a thick, ~1 m, well-developed, pedogenic Km horizon (calcic Stage IV-V). This high mesa has a longitudinal profile at its apex that is about 167 m higher than the adjacent apex of the Cedar Mesa alluvial fan. The center of the mesa is about 275 m above the present stream level of the confluence of Currant and Dry creeks. However, the profile gradient is steeper than Cedar Mesa so that, south of the map area, the elevation of Redlands Mesa closely matches the adjacent Cedar Mesa alluvial fan (Qg7). Noe and others (2015) placed the distal portion of the Redlands Mesa gravel deposit in the Qg7 gravel deposit. Where measured at canal exposures, the gravel is about 35 m thick along the perimeter of the mesa. However, in the interior of the mesa, water wells penetrated over 80 m of basaltic gravel without encountering the underlying Mancos Shale bedrock, likely reflecting the aggradation of sediments into a paleovalley. At the apex of Redlands Mesa alluvial fan, the deposit surface elevation is 138 m above the base level of Leroux Creek. At the southern map boundary, the deposit surface elevation is 161 m above the base level of Leroux Creek. Gravel deposit nine (QNg9) does not occur in the map area. A single remnant was previously mapped as Tg9 just south of the map boundary (Noe and others, 2015b).01-03-08DMUUnit1Qg8Qg8254-251-2210-197-255; 605 breccia openDAS1Alluvial sediment, mostly coarse-grainedHighDMU15
16QNg10Gravel deposit tenGravel deposit tenLower Pleistocene to Upper Pliocene?Basaltic boulder gravel of unit QNg10 forms a high-elevation, massive alluvial fan called Oak Mesa; a portion of which lies in the southeast corner of the map area. Deposits of this unit, including subsequent soil development, are very similar to the deposits of Cedar Mesa (Qg7) and Redlands Mesa (Qg8). However, at the southern map boundary, the surface of Oak Mesa is 240 m in elevation higher than Redlands Mesa of early Pleistocene age and is 385 m above the base level of Leroux Creek. Thicknesses vary; although no water-well data is available, the deposit was measured about 50 m thick overlying Mancos Shale at the south map boundary. However, bedrock was observed at the surface of unit QNg10 in one location where the Rollins Sandstone Member (Kir) is poorly exposed. Although a terrace deposit composed of early North Fork Gunnison River gravel was reported underlying unit QNg10 by Noe and others (2015b), in-situ terrace gravel was not observed by the author during geologic mapping of the Dry Creek quadrangle but may have been obscured by poor exposures. Pebbles of granodiorite porphyry of the West Elk Mountains provenance were seen in hillslope colluvium down slope of Oak Mesa within the map area.01-03-09DMUUnit1QNg10QNg10245-245-1220-92-230; 601 gravel openDAS1Alluvial sediment, mostly coarse-grainedHighDMU16
17QdfDebris-flow depositsDebris-flow depositsHoloceneBrown-gray to tan-gray, clast-supported, poorly sorted, poorly stratified, bouldery deposits formed from transport of rock fragments in a viscous to hyperconcentrated debris-laden flow. The deposit matrix is unsorted sand, silt, and clay. Mancos Shale hillslope morphology suggests soil-slip earth flows may have locally contributed debris to this deposit. Clasts are mostly subangular to rounded basaltic rocks of the GMVF up to 2 m long that have eroded from older Qg deposits. Thickness is unknown, but the deposit contains drainage channels up to 5 m deep. 01-03-10DMUUnit1QdfQdf255-255-190112-168-0; 607 sandDAS1Debris flows, landslides, and other localized mass-movement sedimentHighDMU17
18NoneALLUVIAL-COLLUVIAL DEPOSITSALLUVIAL-COLLUVIAL DEPOSITSNoneNone01-04DMUHeading2NoneNoneNoneNoneDAS1NoneNoneDMU18
19QacAlluvial and colluvial deposits, undividedAlluvial and colluvial deposits, undividedHoloceneTan-gray to olive-gray to dark-gray, sandy to silty clay with sporadic dispersed pebbly gravel that was deposited in a low-energy alluvial and colluvial environment on low-gradient (typically <15°) slopes. Gravel is composed chiefly of basaltic clasts reworked from older gravel and landslide deposits. The sediments are typically deposited by slope rilling and slopewash processes, but locally includes riverine Qg deposits too small to map. Unit is poorly sorted and poorly stratified and is typically deposited along the lower flanks of hillsides and upland valleys in the Williams Fork Formation. In upland valleys, the unit typically contains shallow drainage channels where GMVF basaltic rocks are locally exposed. Unit thickness is highly variable. Localized areas may include bedrock residuum or thicken where unmapped earth-flow sediments may have been incorporated into the deposit. Swelling-soil hazards may occur in clay-rich deposits of this unit where deposits are derived from the weathering of Mancos Shale.01-04-01DMUUnit1QacQac215-215-158255-0-197; 601 gravel openDAS1Alluvial sediment, mostly coarse-grainedHighDMU19
20NoneMASS-WASTING DEPOSITSMASS-WASTING DEPOSITSNoneNone01-05DMUHeading2NoneNoneNoneNoneDAS1NoneNoneDMU20
21QcColluvial depositsColluvial depositsHoloceneOlive-gray to tan-gray rocky sediments on hillsides and swales of mesas and ridgelines, deposited primarily by gravity with limited additions of slopewash sediments. The unconsolidated deposit is typically rocky, poorly sorted, and poorly stratified. Unit is derived from the erosion of upslope bedrock and older gravel units. The boulder- to pebble-sized clasts are dispersed in a sandy clay matrix, but may be locally clast supported where talus forms at the base of steep slopes. Deposit thickness likely does not exceed 3 m, with some deposits ranging from less than 1.5 m to a stony residuum on weathered bedrock slopes at the angle of repose. Swelling-soil hazard may occur where the deposit is clay-rich and derived from Cretaceous shale rocks. 01-05-01DMUUnit1QcQc254-249-194135-183-165; 10% ordered stippleDAS1Colluvium and other widespread mass-movement sedimentHighDMU21
22QcoOld colluviul depositsOld colluviul depositsUpper to Middle PleistoceneOld colluvial deposits that mantle hillsides, mesa risers, and swales on slopes with gradients that may steepen up to the angle of repose, from 10° to 34°. The sediments are reworked from Upper to Early Pleistocene gravel units (Qg4 through QNg10) and exposed bedrock. These deposits are reddish-brown to light tan-gray and moderately consolidated. On flatter slopes, the unit may contain slopewash sediments washed down from exposed bedrock and rocky surficial deposits that cap higher slopes. Unit is unsorted and poorly stratified, containing abundant subangular to subrounded, boulder-sized clasts in a gravelly clay matrix. A well-developed K soil horizon, calic stage III+ - IV, over 1-m thick, forms a chalky-white band exposed in landslide scarps. Where derived from older mesa gravel, weathered basaltic boulders exposed on the surface are heavily stained with desert varnish, fractured, and covered with weathering pits. At the base of near-vertical sandstone outcrops of the Kw and Kir units, the deposit forms aprons of talus and fans of blocky rockslide rubble. Qco deposits are thickest, up to 20 m, on surfaces that include rockslide material. Locally, some deposits are less than 1.5-m thick and may only be a veneer of rocks consolidated within a weathered K-horizon soil matrix that extends into the underlying bedrock. The unit may locally contain unmapped soil-slip landslide deposits. The bouldery deposit armors the slope, and subsequent erosion into softer underlying bedrock has formed triangular-shaped facets on some Qco deposit surfaces.01-05-02DMUUnit1QcoQco254-249-194255-127-127; 10% ordered stippleDAS1Colluvium and other widespread mass-movement sedimentHighDMU22
23QlsrRecent landslide depositsRecent landslide depositsUppermost to Middle HoloceneVariable brown, brown-gray, gray and reddish-gray, unsorted, unstratified, chaotically mixed, deposit of abundant cobble- to boulder-sized basaltic rocks of the GMVF in a matrix of gravelly to silty clay with soft, contorted, plastically deformed, clay-rich sedimentary rock fragments. Recent landslide morphology is commonly observed on hillshaded lidar imagery. Observed landslide forms include relatively fresh and oversteepened scarps and sheared furrows along side slopes, ruptured and fissured ground, rotated slump blocks, pressure ridges, and hummocky to lobate landforms. In the landslide terrain in the northern portion of the map area, Qlsr deposits deform plastically and failed to mobilize as a fluidized flow with extended sinuous runout zones (Qefr). Most of the mapped Qlsr deposits overlie heavily weathered clay-rich Cretaceous and Paleogene rocks. Some Qlsr landslides are historical and were initiated along hillslopes and mesa risers (where shale bedrock is shallow) when lands were developed for agricultural use, and irrigation commenced. Thicknesses are unknown, but likely highly variable depending on the size of the landslide deposit. For land-use purposes, this map unit should be considered to contain potentially active landslides and prone to continuous movement. Where landslide deposits are derived from Cretaceous shales, expansive soils may also occur.01-05-03DMUUnit1QlsrQlsr252-222-88NoneDAS1Debris flows, landslides, and other localized mass-movement sedimentHighDMU23
24QlsiIntermediate landslide depositsIntermediate landslide depositsMiddle Holocene to Upper PleistoceneIntermediate-aged landslide deposits similar in size and composition to Qlsr landslides that can be discerned in hillshaded lidar imagery. However, they have been smoothed and vegetated during extended exposure to weathering and erosion. These deposits are prehistoric, but they may be susceptible to reactivation during periods of high precipitation or if disturbed by ground modifications such as excavations and (or) fill placements. The stability of intermediate-aged landslide deposits is unknown, but they should not be considered dormant. They will likely be sensitive to ground disturbance and (or) the addition of water. Stability analyses should be completed before land use that includes occupied structures.01-05-04DMUUnit1QlsiQlsi215-194-158NoneDAS1Debris flows, landslides, and other localized mass-movement sedimentHighDMU24
25QlsoOld landslide depositsOld landslide depositsUpper to Middle PleistoceneOld landslide deposits typically occur in riser slopes that flank the older mesas (Qg5 through QNg10) that overlie weak clay-rich bedrock. Red-brown topsoil and ≤ 1-m thick chalky-white Bk and K horizons are present. These landslide deposits contain many weathered and pitted basaltic boulders that armor slopes at the surface. The ground morphology is more eroded and smoother compared to that of the Qlsi unit. However, landslide landform morphology is still discernable in hillshaded lidar imagery. Unit thickness is highly variable but likely exceeds 30 m at the landslides on the flanks of Redlands and Oak mesas. Old landslide deposits are generally stable, but they can be sensitive to ground disturbances and (or) the addition of water.01-05-05DMUUnit1QlsoQlso255-202-144NoneDAS1Debris flows, landslides, and other localized mass-movement sedimentHighDMU25
26QefrRecent earthflow depositsRecent earthflow depositsUppermost to Middle HoloceneRecent, variably colored, unsorted landslide deposits composed of very soft, clay-rich, disturbed sedimentary rock, plastically deformed mudstone fragments, and silt and clay. Observed landforms include flow paths, flow banding, hummocks, sinuous lateral side-shear furrows and levees, soil ripples, and lobate toes of the deposit that overthrust (override) and spread over the preexisting ground surface. Boundaries of this unit were predominantly interpreted from hillshaded lidar imagery. Recent earth-flow pathways have undergone little erosion or subsequent ground-movement disturbance. On some of the most recent flows, ruptured, torn, and contorted ground surfaces have not yet been revegetated. Thickness is unknown but likely is highly variable. In the earthflow evacuation zones, weathered and disturbed bedrock may be exposed. A lobate earth-flow toe is up to 10 m above the Dry Creek floor in the Grand Mesa National Forest. These deposits are susceptible to creep and reactivation during periods of high precipitation. Deposits of the Qefr unit are unpredictable, susceptible to continuous movement, and should be considered potentially active when considering land development. 01-05-06DMUUnit1QefrQefr254-249-194143-172-118; 502 periglacialDAS1Debris flows, landslides, and other localized mass-movement sedimentHighDMU26
27QefiIntermediate earthflow depositsIntermediate earthflow depositsLower Holocene to Upper PleistoceneVariably colored, landslide deposits that are mapped where earth-flow pathways are discerned on hillshaded lidar imagery within undivided landslide (Qlsu) deposits. Intermediate earthflow pathways are older than those of unit Qefr, based on a combination of cross-cutting relationships, muting of ground morphology by weathering and erosion, and development of drainage networks on the deposit. Thickness is unknown but likely highly variable. In some upper excavation source areas of earth-flow landslides in the Grand Mesa National Forest, lidar shaded hillside imagery suggests the underlying, potentially disturbed bedrock may be near the surface. These deposits may be susceptible to creep and reactivation during periods of high precipitation and (or) rapid spring snowpack melting.01-05-07DMUUnit1QefiQefi255-255-115255-127-127; 502 periglacialDAS1Debris flows, landslides, and other localized mass-movement sedimentHighDMU27
28QlsuLandslides, undividedLandslides, undividedHolocene to lower Pleistocene?Undivided landslide deposits that mantle slopes in the northern third of the map area where the underlying bedrock is weak, clay-rich Paleogene (:g and :w) formations, and shale intervals of the upper Williams Fork (Kw) Formation. The deposit is typically unsorted, disturbed, plastically deformed mudstone and earth-flow breccia derived from clay-rich bedrock, which also contains abundant, angular to subrounded, basaltic rocks that were mobilized from talus deposits, glacial till, and blockfield deposits to the north below GMVF basalt exposures (White, 2023). Basaltic rock fragments range in size from cobbles to boulders as much as 2.5-m wide. Unit thickness is highly variable. At landslide scarps, bedrock may be shallow, but it is likely to be disturbed. Water-well logs on file at the Colorado DWR shown on the map indicate thicknesses of landslide deposits with entrained basaltic boulders range from 6 to 33 m thick. Early Pleistocene landslide deposits of this unit were the source materials for younger Pleistocene (Qg3 through Qg6) gravel deposits mapped on this quadrangle and adjacent quadrangles (Noe and Zawaski, 2013; Noe and others, 2015a; White and Palkovic, 2019; White, 2023). More recent earth-flow mobilizations and landslide reactivations within this unit, discerned by scarps and ground morphology observed in lidar hillshade imagery, have been mapped separately as units Qefr, Qefi, Qlsr, and Qlsi.01-05-08DMUUnit1QlsuQlsu254-225-128NoneDAS1Colluvium and other widespread mass-movement sedimentHighDMU28
29NoneBEDROCK GEOLOGYBEDROCK GEOLOGYNoneNone02DMUHeading1NoneNoneNoneNoneDAS1NoneNoneDMU29
30PEgGreen River FormationGreen River FormationEoceneGray-white to gray, yellow-tan to light-brown, and light green-gray marlstone, mudstone, very fine- to fine-grained sandstone, limestone, and minor oil shale. This thinly bedded to interlaminated unit records the sedimentation in intermountain lakes during the Eocene. The unit contains both lacustrine and nearshore clastic facies. This formation is more indurated and creates steeper slopes between the conformable interfingering contacts with the underlying, less indurated Wasatch (:w) Formation. However, unit :g is also prone to slope failure; it is almost entirely buried by surficial landslide deposits of Quaternary age and is only exposed in landslide scarps at the northeast corner of the map area. Disaggregation and flow of rock debris from this unit can form long pathways of earth-flow deposits (Qefr) that have moved as much as 2.5 km downslope. Unit thickness is estimated at 230 m.02-01DMUUnit1:gPEg246-191-99NoneDAS1Mostly mudstoneHighDMU30
31PEwWasatch Formation, undividedWasatch Formation, undividedEocene and PaleoceneUndivided, variegated reddish-brown, light-gray, gray, lavender, and maroon mudstone, buff to light-gray weakly cemented sandstone, and shale. This color-banded formation was deposited in a terrestrial environment and is clay-rich and poorly indurated. Predominantly a weak rock unit, the Wasatch Formation is disturbed at the ground surface by mass-movement processes and is poorly exposed within the undivided landslide complex (Qlsu). Unit is only locally exposed in landslides scarps and landslide slopes scoured by erosion. Slopes in the Wasatch Formation at high elevations (≥ 2,500 m above mean sea level (AMSL)) and correspondingly higher (>60 cm) annual annual precipitation are prone to instability and landsliding. Unit thins to the southwest. Thickness is estimated at 400 m.02-02DMUUnit1:wPEw245-162-122NoneDAS1Mostly mudstoneHighDMU31
32KwWilliams Fork FormationWilliams Fork FormationUpper CretaceousBuff to tan, massive, cross-stratified, non-calcareous sandstone and interbedded gray siltstone, dark-gray shale, carbonaceous shale, and basal coal. This unit was formed from sediments in a terrestrial floodplain environment. The top half of the unit is predominantly massive bedded, laterally extensive, cross-stratified sandstone interbedded with thin- to medium-bedded siltstone and shale. Rare, thin shale beds are locally maroon-red. The sandstone is very coarse- to medium-grained, well-sorted, friable, and locally contains ripple marks and lenses of shale rip-up clasts. There are common pebble- to cobble-sized iron-oxide concretions. Contorted, penecontemporaneous load-deformation structures locally occur. Landslides and colluvial surficial deposits cover many areas underlain by Kw bedrock. However, where sandstone is exposed, the upper part of the unit locally forms bench-like outcrops. Down section, the unit contains more shale beds and forms ledgy slopes, composed of stacked sequences of thick mudstone beds and interbedded, laterally discontinuous, channel sandstone beds. Orange-brown concretions, dinosaur tracks, and fossil plants and wood are locally present. In the lower center part of the map area, the basal Cameo-Wheeler coal zone outcrops along a west-to-east trending belt. This zone contains abandoned and reclaimed mine workings. In the coal zone, ancient coal fires have formed prominent red clinker deposits that locally may be encrusted with white mineral precipitate. Thinner ash beds, formed by the subsurface burning of thicker coal seams, locally underlie deformed strata. Clinker types range from reddish-stained but principally unaltered sandstone to dark red displaced collapse breccia fused to form a porcellanite. As mapped, the Kw unit includes the Paleocene and Upper Cretaceous Ohio Creek Formation. Oil and gas well logs in the northwest corner of the map area indicate the Ohio Creek Formation is present with a thickness range of 261 to 297 m. The unit is composed of sandstone and conglomerate containing polylithic quartzite, chert, and minor igneous and metamorphic pebbles and cobbles. Much of the upper strata of the Kw unit is buried by surficial deposits. The total thickness estimated from oil and gas logs is 850 to 1,000 m.02-03DMUUnit1KwKw51-196-90NoneDAS1Sandstone and mudstoneHighDMU32
33KirRollins Sandstone Member of the Iles FormationRollins Sandstone Member of the Iles FormationUpper CretaceousGray-white to tan to pale-orange, fine- to medium-grained, thick- to massive-bedded, cross-stratified sandstone deposited as sandy sediment in a nearshore to shoreface marine environment. Where it is not covered by expansive gravel-capped mesas, the exposed Kir unit weathers to form landforms that range from benchy cliffs to, more commonly, an upper 30.5-m tall continuous vertical cliff that forms a prominent, northward-sloping cuesta. The massive upper section consists of low-angle crossbedded sandstone capped by subhorizontal bedded sandstone. In the top third of the unit, sandstone is commonly bleached gray-white, is increasingly friable, and has a slick-rock appearance that helps make it a prominent marker bed in outcrop. Marine mollusk fossils (Inoceramid sp.) and burrow trace fossils are locally present, most common in orange-tan, coarse-grained, calcite-cemented, medium-thick beds. The sandstone unit’s upper contact locally may be stained red from ancient coal fires within the Cameo-Wheeler coal zone of the overlying Williams Fork Formation. Lower in the section below the 30-m massive sandstone, sandstone is very fine-grained with hummocky and swaley crossbedding. Bedding is thinner, somewhat bioturbated, and increasingly interbedded with silty marine shale. This basal, thinly bedded interval is thickest and best exposed at the cuesta exposure between Currant and Dry creeks. The basal contact of this unit was mapped at the first sandstone bed that is conformably interbedded with the underlying Mancos Shale tongue of the Kicz member unit. Total thickness ranges from 45 to 70 m.02-04DMUUnit1KirKir117-176-88NoneDAS1SandstoneHighDMU33
34KiczCozzette Sandstone and tongue of Mancos Shale members of the Iles FormationCozzette Sandstone and tongue of Mancos Shale members of the Iles FormationUpper CretaceousLight orange-brown to tan-brown, coarsening-upward, very fine- to medium-grained, locally bioturbated sandstone with swaley cross-bedding and basal, interlaminated to very thin interbeds of sandy shale. Unit Kicz includes the Mancos Shale tongue interval between the Cozzette and the Rollins (Kir) sandstone members. The Cozzette Sandstone is best exposed where it outcrops in Cactus Park as a 5 m-thick sandstone bed that fines downward to dark-gray siltstone. The sandstone unit thins considerably to the east and becomes a very poorly exposed, <1 m-thick sandstone bed and concretion horizon. Conversely, the Mancos Shale tongue of the Kicz unit thickens to the east (Dunrud, 1989). In the Dry Creek valley, the unit's base is approximated by a prominent light-gray horizon that weathers in the Mancos Shale slope exposures below the Kir unit. Thickness is about 55 m at Cactus Park, thickening to about 105 m in the Dry Creek valley exposure.02-05DMUUnit1KiczKicz209-255-115NoneDAS1Sandstone and mudstoneHighDMU34
35NoneMancos ShaleMancos ShaleUpper CretaceousThe Mancos Shale is present in the southern part of the quadrangle exposed in valleys and mesa risers and typically capped by Qg gravel deposits or buried by valley-fill deposits (Qaf). Hillslopes of Mancos Shale are susceptible to instability and are locally disturbed by landslides. Twelve members of this marine shale, distinguished on the basis of composition, color, and fossil assemblages were mapped in the bordering Orchard Mesa, North Delta, and Lazear quadrangles (Noe and Zawaski, 2013; Noe and others, 2015a; Noe and others, 2015b). Only the upper Mancos unit (Kmu) and the tongue of Mancos shale included within the Kicz unit occurs within the Dry Creek quadrangle. On mesas risers and ridgelines, the gray to dark-gray shale typically contains an oxidized, yellow-tan stained horizon that is highly fractured with crystalline gypsum fracture filling. This approximately 9- to 15-m thick weathered interval, once subaerially exposed and subsequently buried by Pleistocene surficial deposits, has been informally referred to as the Mancos "blonde" by local Natural Resources Conservation Service soil scientists. In the map cross section (Plate 2), the Mancos Shale is undivided. The Mancos Shale has thin bentonite beds and may locally contain expansive clay minerals; swelling-soil hazards may occur locally.02-07DMUUnit1NoneNoneNoneNoneDAS1NoneNoneDMU35
36KmuMancos Shale, upper partMancos Shale, upper partUpper CretaceousDark-gray to olive-gray, non-calcareous, fissile to subblocky, silty to sandy shale. Unit contains scattered, orange-brown concretions up to 3.5 m long along bedding. Many of the concretions are septarian with calcite fracture filling. The unit locally contains thin cream-colored bentonite seams, and marine invertebrate mollusk and gastropod fossils. Unit thickness is about 330 m (Noe and others, 2015b).02-08-01DMUUnit1KmuKmu185-186-145NoneDAS1MudstoneHighDMU36
37KmMancos Shale, undividedMancos Shale, undividedUpper CretaceousShown in cross section only.02-08-02DMUUnit1KmKm220-222-216NoneDAS1MudstoneHighDMU37
38KdbDakota Sandstone and Burro Canyon Formation, undividedDakota Sandstone and Burro Canyon Formation, undividedUpper to Lower CretaceousShown in cross section only02-09DMUUnit1KdbKdb186-170-126NoneDAS1Sandstone and mudstoneHighDMU38
39MzMesozoic Formations, undividedMesozoic Formations, undividedJurassic and TriassicMajor units include the Morrison Formation, Entrada Sandstone, and Chinle Formation. Shown in cross section only.02-10DMUUnit1MzMz177-209-223NoneDAS1Sedimentary rockHighDMU39
40pCPrecambrian rocks, undividedPrecambrian rocks, undividedProterozoicCrystalline igneous and metamorphic rocks. Shown in cross section only.02-11DMUUnit1=pC179-153-153NoneDAS1Igneous and metamorphic rockHighDMU40
41waterwaterwaterHolocenewater03DMUHeading1waterwater190-232-255 fill, 0-0-255 outlineNoneDAS1Water or iceHighDMU41

Glossary

OBJECTIDTermDefinitionDefinitionSourceIDGlossary_ID
13AGEthe length of time during which a being or thing has existed; length of life or existence to the time spoken of or referred toDICT1GLO11
14BeddingAttitudeThe orientation of a structural element (plane or line) relative to a horizontal plane. Attitudes of planes are expressed by strike and dip (or dip direction and dip), whereas attitudes of lines are expressed by bearing (or trend, azimuth) and plunge.AGI1GLO12
22borderThe edge or boundary of something, or the part near itDICT1GLO20
8boundaryA line that marks the limits of an areaDICT1GLO01
1certainIdentity 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-013-2006GLO02
15Clinker(a) Sandstone and mudstone bedrock that has been altered by the heat from burning of interbedded or nearby coal seams (b) Coal that has been altered by igneous intrusion. Cf: natural coke. Syn: scoria [coal]. (c) Masses of coal ash that are a byproduct of combustion. Cf: coke.AGI1GLO13
23coal mine spoilsA nonspecific term typically referring to overburden, non-ore, or other waste material produced in mining, quarrying, dredging, excavating, construction, and other operations involving earth modification.AGI1GLO21
9contactA plane or irregular surface between two types or ages of rock; examples are faults, intrusive borders, bedding planes separating distinct strata, and unconformities. AGI1GLO03
16Cross Section(a) A diagram or drawing that shows features transected by a given plane; specif. a vertical section drawn at right angles to the longer axis of a geologic feature, such as the trend of an orebody, the mean direction of flow of a stream, or the axis of a fossil. Cf: longitudinal section. Syn: transverse section. AGI1GLO14
17DEPOSIT TYPEGroupings for surficial units in the CMUDAS1GLO15
5DMUHeading1GeMS hierarchy formatting termGEMS1GLO04
6DMUHeading2GeMS hierarchy formatting termGEMS1GLO05
7DMUUnit1GeMS hierarchy formatting termGEMS1GLO06
18ELEVA hatch mark shown on the edges of geologic cross sections to denote the elevationDAS1GLO16
12faultA discrete surface or zone of discrete surfaces separating two rock masses across which one mass has slid past the other. AGI1GLO07
10fault, concealedA discrete surface or zone of discrete surfaces separating two rock masses across which one mass has slid past the other. Concealed indicates that the existence is certain and the location is concealedAGI1GLO08
11fault, inferredA discrete surface or zone of discrete surfaces separating two rock masses across which one mass has slid past the other. Concealed indicates that the existence is questionable and the location is inferredAGI1GLO09
19FRAMEA border enclosing the cross section dataDICT1GLO17
24gravel pitAn open-pit mine for the extraction of gravel. AGI1GLO22
28Highunusual or considerable in degree, power, intensity, etc. DICT1GLO26
25minen. (a) An underground excavation for the extraction of mineral deposits, in contrast to surficial excavations such as quarries. The term is also applied to various types of open-pit workings. (b) The area or property of a mineral deposit that is being excavated; a mining claim. v. To excavate for and extract mineral deposits or building stone.AGI1GLO23
20OandG wellAn oil well is a drilled well to a stratigraphic interval from which petroleum is obtained by pumping or by natural flow. A gas well is a well that is capable of producing natural gas or that produces chiefly natural gas.AGI1GLO18
2questionableIdentity 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-013-2006GLO10
26scarp(a) A line of cliffs or oversteepened slopes produced by landsliding, faulting, or by erosion. The term is an abbreviated form of escarpment, and the two terms commonly have the same meaning, although "scarp" is more often applied to cliffs formed by faulting and landsliding. See also: fault scarp; erosion scarp. (b) A relatively straight, clifflike face or slope of considerable linear extent, breaking the general continuity of the land by separating surfaces lying at different levels, as along the margin of a plateau or mesa. A scarp may be of any height but does not describe properly a slope of highly irregular outline. Cf: scarp slope. (c) beach scarp. (d) The headscarp of a landslide.AGI1GLO24
21USGS coal boringInvestigative drill hole in the earth to determine depth, thickness, and quality of a prospective coal resource. In this case, the USGS bored into a coal deposit and provided information about the coal from the cuttings.AGI1GLO19
27water well(a) A well that extracts water from the saturated zone or that yields useful supplies of water. (b) A well that obtains groundwater information or that replenishes groundwater. (c) A well drilled for oil but yielding only water.AGI1GLO25

MiscellaneousMapInformation

OBJECTIDMapPropertyMapPropertyValueMiscellaneousMapInformation_ID
1PHYSIOGRAPHIC SETTINGThe Dry Creek quadrangle lies in Delta County in western Colorado. The map center lies approximately 10 km northeast to east of the town of Cedaredge. The steeper slopes in the upper third of the map area are part of the southern flank of Grand Mesa and are characterized by high elevations and hummocky, south-facing slopes underlain by landslide deposits. The upper hummocky terrain transitions southward to cliffy mid-elevation sandstone outcrops of the Williams Fork and Iles Formations of the Mesa Verde Group. In the lower valleys and south part of the map area, bouldery gravel underlies low gradient mesa and river terrace surfaces. The highest elevation of the Dry Creek quadrangle is 3,097.0 m (10,160.8 ft) above mean sea level (AMSL) at the northeast map corner within high elevation landslide terrain in the Grand Mesa National Forest. The lowest elevation is 1,850.3 m (6,070.5 ft) AMSL near the southwestern corner of the map area where Current Creek exits the quadrangle, 1.3 km below its confluence with Dry Creek. The annual precipitation in the map area (National Centers for Environmental Information) ranges from about 100 cm along the northern map area where alpine forests are predominant, through a mid-elevation semi-arid Gambel oak, pinyon-juniper, woodland climate of the high alluvial mesas, and to a low of about 33 cm at lower elevations shrublands on the southwest flank of the map area. A winter snowpack occurs in the high country of the map area, and average temperatures are cooler than those along the Gunnison River Valley and in the Grand Junction-Grand Valley area below the confluence with the Colorado River.MMI01
2GEOLOGIC SETTING 1The early Cenozoic and Late Cretaceous evolution of western Colorado is recorded in the transition from marine to terrestrial rocks exposed in the map area. The basal bedrock unit exposed in the map area is the upper member of the Late Cretaceous Mancos Shale. This marine shale was deposited during the Cretaceous Western Interior Seaway (WIS) transgression into west-central North America. Regressive and transgressive sequences of the western shoreline of the WIS formed the sediments of the Iles Formation in shoreface and nearshore environments (Roberts and Kirschbaum, 1995). Of note is the 30-m high gray-white cliffs of the Rollins Sandstone Member that is a prominent stratigraphic marker bed in the area. As the paleoshoreline regressed to the east, broad floodplain environments were created. Sand, mud, and organic-rich swamp sediments, transported from west to southwest sources, formed the Late Cretaceous Williams Fork Formation. Commercial coal deposits in the Cameo-Wheeler coal zone were formed. Uplifts during the Laramide orogeny (of Late Cretaceous and Paleogene ages) occurred along the Southern Rocky Mountain orogenic belt in central Colorado. Concurrently, structural intermountain basins such as the Piceance Basin developed. The resultant erosion of the highlands of the orogenic belt shed deposits of sand, mud, and coarse pebble to cobble gravel that become the sandstone and conglomerate of the Ohio Creek Formation. Later, beginning in the Paleocene, thick packages of terrestrial clastic sediments accumulated to form _____MMI02
3GEOLOGIC SETTING 2the Wasatch Formation. Differential uplift during the Laramide orogeny created closed, structural basins where freshwater lakes formed. The Wasatch Formation sediments were buried by a package of lacustrine and lake-shoreface sediments that formed the Green River Formation of Eocene age (Franczyk and others, 1992). After limited deposition of terrestrial sediments that buried the Green River Formation during the late Miocene, drainage integration led to the establishment of the paleo Colorado River drainage basin on a subdued landscape. Basaltic lava of the Grand Mesa Volcanic Field (GMVF) flowed into this drainage basin during the Miocene (Cole and others, 2017). The GMVF is composed of very hard basaltic bedrock that is resistant to erosion compared to the underlying softer Neogene and Paleogene bedrock (Green River and Wasatch Formations). During late Neogene time, epeirogenic uplift of the Colorado Plateau occurred, possibly coupled by mantle buoyancy and subsequent erosional-isostatic rebound driven in part by regional denudation from river incision by the Colorado River and its Gunnison River tributary. About 1.5 km of regional, late Neogene to Quaternary downcutting by the Colorado River and its tributaries, accompanied by topographic inversion of the resistant GMVF basalt, formed Grand Mesa and nearby Battlement Mesa (Aslan and others, 2019). Major Quaternary events included continuing incision and regional lowering of the landscape, Pleistocene glaciation on Grand Mesa, and mass wasting. The latter continued through the Holocene to the present day. The primary mechanism of topographic lowering is continual ground instability and mass-wasting processes on the flanks of Grand Mesa. Slump blocks, scarps, disturbed and broken ground, heave and pressure ridge features, and linear earth-flow pathways are typical of the upper slopes that surround the Grand Mesa rim (Baum and Odom, 1996; White and Palkovic, 2018; Chesnutt and others, 2018; White and Palkovic, 2019; and White, 2023). The source materials for much of the landslide deposits are GMVR basaltic rocks from blockfields, glacial till, and glacio-fluvial outwash, and the underlying weak clay-rich Neogene and Paleogene sedimentary rocks. Episodes of erosion and alluvial deposition, likely related chiefly to glacial and interglacial events during the Pleistocene, shed rocky alluvial sediments from the highland terrain. This material was mainly deposited in large aprons of bouldery alluvial-fan gravel and very rocky debris-flow deposits at and near the base of the landslide terrain. Water-well logs suggest that basaltic gravel filled paleovalleys. For example, the maximum recorded thickness of the gravel on Cedar Mesa was 66 m (White, 2023), and one water well on Redlands Mesa exceeded 80 m, far thicker than measured exposures along the mesa perimeters. Subsequent erosion and ground-surface lowering have resulted in the formation of gravel-capped mesas. The most distinctive, from the highest and oldest gravel in the map area, caps Oak Mesa, Redlands Mesa, and Cedar Mesa, which all display alluvial-fan morphology on topographic maps and lidar hillshade imagery. Younger terrace gravel treads occur within stream valleys whose basins extend to the highlands. All the mesas, mesa remnants, and river terraces have longitudinal profiles that slope southward towards the Gunnison River Valley.MMI03
4GEOLOGIC SETTING 3The structural geology of the Dry Creek quadrangle reflects the regional development of Late Cenozoic basins. Formations generally dip at a gentle grade away from the Uncompahgre Plateau Uplift towards the Piceance Basin to the north. Structural data, such as bedding attitudes, was difficult to obtain because of extensive Quaternary surficial deposits that cover the underlying bedrock and (or) subsidence and collapse deformation near clinker zones in exposed Williams Fork strata resulting from coal seam fires in the Cameo coal zone. The only structural feature observed by the author in the map area is a normal fault that offsets the Rollins Sandstone, which trends northwestward and crosses LeRoux Creek, where the valley broadens and is underlain by Mancos Shale. No other surface expressions of other faults, no strata offsets, nor deformation-band damage zones typically seen in faulted sandstone were observed. However, Hail (1972) shows a short fault that offsets Wasatch and Williams Fork formations high on the slopes north of Leroux Creek, which this author could not discern within the landslide deposits in that area. Dunrud (1989) mapped several inferred faults in his study of the coal-bearing strata exposed in the Dry Creek quadrangle area, mostly along river valleys and canyons that cut into the Rollins Sandstone and Williams Fork Formation. Structure-contour offsets drawn by Dunrud (1989) at the top of the Rollins Sandstone (Kir) are in areas covered by thick surficial deposits; so were likely inferred from coal exploration well logs. Regionally, the map area lies upon the trend of the ancestral Pennsylvanian-Permian Uncompahgre Uplift where the entire package of Paleozoic rocks was removed by erosion before the deposition of Mesozoic and Cenozoic sediments. An oil and gas well log (API No. 05-029-05030) shown in the southeast quadrant of the map area near Leroux Creek logged the nonconformity between the Mesozoic rocks and Precambrian crystalline rocks at a depth of 1,484 m (560 m AMSL).MMI04
5WATER RESOURCESThe southern flank of Grand Mesa just north of the Dry Creek quadrangle contains major watersheds that flow southward into the map area. The upper watersheds along the high flanks (about 3,200 m AMSL) receive high (about 125 cm) annual precipitation, much of which is stored in winter snowpack. The watersheds are a critical water resource for domestic and agricultural use, recognized by Delta County Board of County Commissioners (Kolm and van der Heijde, 2014). Almost all pastures, orchards, vineyards, and crop farmland are irrigated. Surface Creek and Leroux Creek provide water to public water systems (PWS), and current rules (Colorado Energy and Carbon Management Commission (ECMC) rule 411.a) have buffered creek areas from oil and gas activity in the map area to protect water quality. Almost all privately owned completed water wells draw water from thick unconsolidated deposits, some are landslide deposits, but most are gravelly alluvium on the mesas or along terraces treads in incised valleys. Selected water wells from the DWR water-well database are shown on the map to indicate gravel thickness. The underlying rock units do not produce much water. Seasonal recharge of groundwater in the gravel mesas occurs from watersheds that extend north of the map area.MMI05
6MINERAL RESOURCESOil and gas, coal, coal-bed methane, and clinker shale are potential and current mineral resources in the Dry Creek quadrangle. Coal resources exist in the basal part of the Williams Fork Formation (Cameo-Wheeler coal zone) within the map area (Lee, 1912), which were developed in the early- to mid-1900s. The coal zone and related red clinker beds outcrop in a band directly above the Rollins Sandstone. The outcrop trends west to east near the lower middle of the map area where the high Rollins Sandstone cuesta is prominently exposed above Cactus Park and in the valleys of Currant, Dry Creek, and Leroux creeks before the valleys broaden where underlain by the more easily eroded Mancos Shale. At the east boundary of the map area, the outcrop follows the riser of Oak Mesa and ends where the high gravel surface buries bedrock strata. Coal beds up to 4-m thick have been reported (Lee, 1912). Dunrud (1989) reported deep coal-resource test borings identifying multiple coal seams. Some of those boring locations are shown on the map (Eager, 1978 and 1979). Several small coal mines that historically operated in the map area are now closed and the mined land has been reclaimed. Within the coal-mining district, there are small quarries where red clinker rock was mined. There has been some oil and gas drilling activity within the map area. In the northwest corner of the map area, wells were completed in Cretaceous rocks at a small gas field near Surface Creek. During the preparation of this map, these wells were either plugged and abandoned or shut-in (ECMC). Coal-bed methane within the Williams Fork Formation and the Mancos Shale Niobrara Member may have gas potential using horizontal well drilling and hydraulic fracturing completion techniques. The coal-bearing units dip northward. Oil and gas well logs (COGCC COGIS) place the top of the Cameo coal zone about 850 m deep (1,750 m AMSL) at the northwestern corner of the map area. Except for the red clinker quarry mentioned earlier, the aggregate resource value of the extensive gravel deposits is limited because they commonly have layers of mud and poorly sorted debris-flow gravel that contain weak sedimentary clasts as well as high percentages of clay and silt. There are a few borrow pits in the map area. Opportunities may exist for the collection of weathered and pitted boulders suitable for landscaping stone that are common in the map area, particularly within the main drainage basins in the map area. Boulders are commonly moved to the sides of agricultural fields and removed from foundation and borrow-area excavations.MMI06
7GEOLOGIC HAZARDSPotential geologic hazards in the map area are primarily the risk posed by landslides and other ground movements; however, there are also areas susceptible to rockfall, debris-flow flooding, and coal-mine subsidence hazards. The Mancos Shale also contains bentonite and other expansive clay minerals. Clayey surficial sediments derived from the shale may be expansive (and referred to as swelling soils). The marine shale may also be high in sulfates, which can be corrosive to unprotected concrete and steel. Site-specific geotechnical investigations, including boreholes and soil testing, should be conducted for structures planned in the Mancos Shale or clayey soils that are derived from it. Landslides are ubiquitous throughout the northern part of the map area. Lands within the northern mapped landslide areas, underlain by the weak clay-rich Neogene and Paleogene rocks, are predominantly undeveloped and unoccupied public lands or private ranch land. Several areas in this terrain are actively moving down slope. In the lower terrain, most mesa flanks or risers underlain by Mancos Shale are also susceptible to landsliding. The mesa tops are irrigated, and where the gravel is underlain by shale, irrigation water percolates down to the water table and moves laterally along the contact between the permeable gravel and the underlying impermeable shale. Many ancient to recent landslides are mapped along the flanks of high mesas where wet ground conditions previously occurred on the steeper slopes as stream downcutting continued through the Pleistocene into the Holocene. The near-vertical scarps of fresh landslides expose gravel, and underlying weak shale may also be exposed. At older landslides, the scarp is covered by old colluvial deposits. Areas of mapped landslides and earthflows should be considered susceptible to future ground movements. Careful geological and geotechnical investigations should be completed for any site within mapped landslide areas if land-use changes and critical, permanent, and (or) occupied structures are planned. Those investigations would also be warranted for prospective buyers of real estate within mapped landslides, especially if residential structures exist or are being planned. Earth flows and debris flow/flash flooding can have long runouts (as much as 2.5 km). Careful planning and siting of structures are also important in the vicinity of creek floors and drainage swales. This map only shows existing landslides and earthflows, and does not reflect future risk or recurrence intervals for ground movements. Future landsliding could occur in any susceptible area along the flanks of Grand Mesa and hillsides adjacent to gravel-mantled mesas in the map area. Those ground movements can range from slow, nearly imperceptible, creep to movements that destroy structures to dangerous, potentially catastrophic rock avalanche-type flows. Rockfall hazards occur along the base of high, near-vertical sandstone cliffs (e.g., Rollins Sandstone) or any cliffy slope with a steep grade (slope) that exceeds the angle of repose. Debris flow and hyperconcentrated flash flooding may also be hazards where drainage channels lie within steep terrain and outlet onto alluvial or debris-flow fans. Several small historic underground coal mines exist in the map area. Coal-mine subsidence should be considered prior to future construction above underground workings.MMI07
8PREVIOUS GEOLOGIC MAPPINGThe preparation of this map was aided by the review of previous geologic mapping conducted in the area. The geology of the Dry Creek quadrangle was previously mapped at limited, small-scale extents by Lee (1912) in a 1:125,000-scale plate that accompanied his report on the Grand Mesa coal field; at 1:250,000 scale by Williams (1964); and at 1:50,000 scale by Dunrud (1989) who mapped coal-bearing rocks. Hail (1972) mapped a 15-minute quadrangle (scale 1:48,000) that includes the Dry Creek area. Quaternary surficial units were previously mapped at a small scale within the map area by Cole and Sexton (1981). Geology has been mapped on adjacent 1:24,000-scale quadrangles as part of this multi-year mapping program by the Colorado Geological Survey. These maps include portions of Grand Mesa and include the Lands End (White and Palkovic, 2018), Mesa Lakes (Chesnutt and others, 2019), Hells Kitchen (White and Palkovic, 2019), and Cedaredge (White, 2020) quadrangles. To the south of the map area along the Gunnison River Valley are geologic maps of the North Delta (Noe and others, 2015a), Orchard Mesa (Noe and Zawaski, 2013), Lazear (Noe and others, 2015b), and Hotchkiss (Noe and Rodgers, 2014) quadrangles. These 1:24,000-scale quadrangles are shown on the Plate 1 index map. MMI08
9ACKNOWLEDGMENTSThe author thanks the following property owners for allowing or facilitating access to critical land parcels for the mapping of Dry Creek quadrangle: U.S. Forest Service - Grand Mesa National Forest; U.S. Bureau of Land Management; Laura and William Vaughn, Vaughn Ranch; Paul Smith, manager of ST Ranches; Mike Ludlow, manager of Bear Ranch; Dennis Durmas, manager for Carlson Ranch; Overland Ditch Co. board members; the Girling family; Hank and Charlie Warren; and Justin Heiber at Cactus Park Ranch. Carrie Derco, the Delta County GIS Coordinator, provided digital 9-inch (23 cm) pixel orthorectified aerial photography and tax assessor land parcel datasets. 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. MMI09
10REFERENCESAslan, A., Karlstrom, K.E., Kirby, E., Heizler, M.T., Granger, D.E., Feathers, J.K., Hanson, P.R., and Mahan, S.A., 2019, Resolving time-space histories of Late Cenozoic bedrock incision along the Upper Colorado River, USA, Geomorphology, vol. 347, 24 p., URL: https://doi.org/10.1016/j.geomorph.2019.106855 Baum, R.L., and Odum, J.K., 1996, Geologic map of slump-block deposits in part of the Grand Mesa area, Delta and Mesa Counties, Colorado: U.S. Geological Survey Open-file Report 96-017, 12 p., 2 plates, scale 1:24,000. https://doi.org/10.3133/ofr9617 Chesnutt, J.M., Wegmann, K.W., Pawl, T.A., White, J.L., Cole, R.D., and Byrne, P.K., 2019, Geologic Map of the Mesa Lakes quadrangle, Mesa and Delta Counties, Colorado: Colorado Geological Survey Open-file Report 19-08, scale 1:24000. Cole, R.D., and Sexton, J.L., 1981, Pleistocene surficial deposits of the Grand Mesa area, Colorado, in Epis, R.C., and Callender, J.F., eds., Western Slope Colorado: New Mexico Geological Society Guidebook, 32nd Field Conference, p. 121-126. https://doi.org/10.56577/FFC-32.121 Cole, R., Stork, A., Hood, W. and Heizler, M., 2017, Geochemical and geochronological characterization of Grand Mesa Volcanic Field, western Colorado, pp. 103-113, in: Karlstrom, K. E., Gonzales, D. A., Zimmerer, M, J. Heizler, M., Ulmer-Scholle, D. S., The Geology of the Ouray-Silverton Area: New Mexico Geological Society 68th Annual Fall Field Conference Guidebook, 219 p. https://doi.org/10.56577/FFC-68. Colorado Division of Water Resources, DWR Well Permit Research Viewer, URL: https://gis.colorado.gov/dnrviewer/Index.html?viewer=dwrwellpermit. Colorado Energy and Carbon Management Commission (ECMC), Colorado Energy and Carbon Management Information System (COGIS). URL: https://ecmc.state.co.us/data.html Dunrud, C.R., 1989, Geologic map and coal stratigraphic framework of the Cedaredge area, Delta County, Colorado: U.S. Geological Survey Coal Investigation Map C-116, scale 1:50,000. https://doi.org/10.3133/coal116 Eager, G.P., 1978, Geophysical logs of coal text drill holes in the Grand Mesa Coal Field, Delta and Mesa Counties, Colorado: U.S., Geological Survey Open-File Report 78-540, 97 p. Eager, G.P., 1979, Geophysical logs of coal text drill holes in the Grand Mesa Coal Field, Delta County, Colorado: U.S., Geological Survey Open-File Report 79-327, 21 p. Franczyk, K.J., Fouch, T.D., Johnson, R.C., Molenaar, C.M., and Cobban, W.A., 1992, Cretaceous and Tertiary paleogeographic reconstructions for the Uinta-Piceance study area, Colorado and Utah: U.S. Geological Survey Bulletin 1787-Q, 37 p. https://doi.org/10.3133/b1787Q Hail, W.J., Jr., 1972, Reconnaissance geologic map of the Cedaredge area, Delta County, Colorado: U.S. Geological Survey miscellaneous geologic investigation map I-697, scale 1:48,000. https://doi.org/10.3133/i697 Kolm, K.E., van der Heijde, P.K.M., 2014, Groundwater systems in Delta County, Colorado: Surface Creek valley area, prepared for Delta County Board of County Commissioners, Colorado, 58 p., URL: http://www.chc4you.org/wp-content/uploads/2017/01/Surface-Creek-Hydrology-Report-2014.pdf Lee, W.T., 1912, Coal fields of Grand Mesa and the West Elk Mountains, Colorado: U.S. Geological Survey Bulletin 510, 237 p. https://doi.org/10.3133/b510 Machete, M.N., 1985, Calcic soils of the southwestern United States in Soils and Quaternary Geology of the Southwestern United States, D.L. Weide and M.I. Faber, eds: Geological Society of America Special Paper 203, p. 1-21. DOI: https://doi.org/10.1130/SPE203 Matthews, N.E., Vázquez, J.A.; Calvert, A.T., 2015, Age of the Lava Creek supereruption and magma chamber assembly at Yellowstone based on 40Ar/39Ar and U-Pb dating of sanidine and zircon crystals: Geochemistry, Geophysics, Geosystems, v. 16, p. 2508–2528, accessed June 2023, at https://doi.org/10.1002/2015GC005881 National Centers for Environmental Information (NCEI), National Oceanic and Atmospheric Administration, URL: https://www.ncdc.noaa.gov/data-access/land-based-station-data/land-based-datasets/climate-normals/1981-2010-normals-data Noe, D.C., and Zawaski, M.J., 2013, Geologic map of the Orchard City quadrangle, Delta County, Colorado: Colorado Geological Survey Open-file Report 13-02, scale 1:24,000. Noe, D.C., and Rodgers, E.L, 2014, Geologic Map of the Hotchkiss quadrangle, Delta County, Colorado: Colorado Geological Survey Open-file Report 14-15, scale 1:24,000. Noe, D.C., White, J.L., and Nelson, M., 2015a, Geologic map of the North Delta quadrangle, Delta County, Colorado: Colorado Geological Survey Open-file Report 15-09, scale 1:24,000. Noe, D.C., Logan, Z.D., McCall, K.J., and Warden, G.W., 2015b, Geologic map of the Lazear quadrangle, Delta County, Colorado: Colorado Geological Survey Open-file Report 15-08, scale 1:24,000. Roberts, L.N.R., and Kirschbaum, M.A., 1995, Paleogeography of the Late Cretaceous of the Western Interior of middle North America—Coal distribution and sediment accumulation: U.S. Geological Survey Professional Paper 1561, 116 p. https://doi.org/10.3133/pp1561 Sturchio, N.C., Pierce, K.L., Murrell, M.T., and Sorey, M.L., 1994, Uranium-series ages of travertines and timing of the last glaciation in the northern Yellowstone area, Wyoming-Montana: Quaternary Research, v. 41, p. 265-277. https://doi.org/10.1006/qres.1994.1030 Wentworth, C.K., 1922, A scale of grade and class terms for clastic sediments: The Journal of Geology. vol. 30, No. 5, pp. 377-392. White, J.L. and Palkovic, M.J., 2018, Geologic map of the Lands End quadrangle, Mesa County, Colorado: Colorado Geological Survey Open-file Report 18-03, scale 1:24,000. White, J.L., and Palkovic, M.J., 2019, Geologic map of the Hells Kitchen quadrangle, Mesa and Delta Counties, Colorado: Colorado Geological Survey Open-file Report 19-05, scale 1:24,000. White, J.L., 2023, Geologic map of the Cedaredge quadrangle, Delta Counties, Colorado: Colorado Geological Survey Open-file Report 20-04, scale 1:24,000. Williams, P.L., 1964, Geology, structure, and uranium deposits of the Moab quadrangle, Colorado and Utah: U.S. Geological Survey I-360, scale 1:250,000. https://doi.org/10.3133/i360MMI10
11TITLEGEOLOGIC MAP OF THE DRY CREEK QUADRANGLE, DELTA COUNTY, COLORADOMMI11
12YEAR2024MMI12
13STATEMAP AGREEMENT NUMBERThis 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 G20AC00245MMI13
14AUTHORJonathan L. WhiteMMI14
15DOI LINKhttps://10.58783/cgs.of2103.ovbr9253MMI15
16OPEN FILE NUMBEROF-21-03DMMI16

Database Inventory

This summary of database content is provided as a convenience to GIS analysts, reviewers, and others. It is not part of the GeMS compliance criteria.

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