Maui, the second largest island in the Hawaiian group, is 48 miles long, 26 miles wide, and covers 728 square miles. The principal town is Wailuku. Sugar cane and pineapples are the principal crops. Water is used chiefly for irrigating cane. The purpose of the investigation was to study the geology and the ground-water resources of the island.
Maui was built by two volcanoes. East Maui or Haleakala Volcano is 10,025 feet high and famous for its so-called crater, which is a section of Hawaii National Park. Evidence is given to show that it is the head of two amphitheater-headed valleys in which numerous secondary eruptions have occurred and that it is not a crater, caldera, or eroded caldera. West Maui is a deeply dissected volcano 5,788 feet high. The flat Isthmus connecting the two volcanoes was made by lavas from East Maui banking against the West Maui Mountains. Plate 1 shows the geology, wells, springs, and water-development tunnels. Plate 2 is a map and description of points of geologic interest along the main highways. Volcanic terms used in the report are briefly defined. A synopsis of the climate is included and a record of the annual rainfall at all stations is given also. Puu Kukui, on West Maui, has an average annual rainfall of 389 inches and it lies just six miles from Olowalu where only 2 inches of rain fell in 1928, the lowest ever recorded in the Hawaiian Islands. The second rainiest place in the Territory is Kuhiwa Gulch on East Maui where 523 inches fell during 1937. Rainfall averages 2,360 million gallons daily on East Maui and 580 on West Maui. Ground water at the point of use in months of low rainfall is worth about $120 per million gallons, which makes most undeveloped supplies valuable.
The oldest rocks on East Maui are the very permeable primitive Honomanu basalts, which were extruded probably in Pliocene and early Pleistocene time from three rift zones. These rocks form a dome about 8,000 feet high and extend an unknown distance below sea level. Covering this dome are the Kula volcanics, extruded probably in early and middle Pleistocene time, and characterized by andesites, andesitic basalts, and picritic basalts. They are 2.000 feet thick on the summit and 50 to 200 feet thick at the periphery. They contain a sufficient number of interbedded soils, thin vitric tuff beds, and lava-filled valleys in their upper part to give rise to valuable perched springs in wet areas. The Kula lavas accumulated during a waning volcanic phase which was followed by a quiescence long enough for the erosion of deep amphitheater-headed valleys in the east or wet half of the mountain. Volcanic activity was renewed in middle (?) to late Pleistocene time and continued until Recent time, during which the Hana volcanic series was laid down. The last lava flow was erupted about 1750. The Hana lavas comprise andesitic, picritic, and olivine basalts. They veneered large areas of the east and south slopes, partly filled the deep amphitheater-headed valleys, and deeply buried the smaller valleys in the eastern half of the mountain. The Hana rocks are exceedingly permeable and much rain sinks into them.
The oldest rocks on West Maui are the very permeable primitive Wailuku basalts, which were extruded probably in Pliocene and early Pleistocene time from two rifts and from many radial fissures. The basalts form a dome about 5,600 feet high and extend an unknown distance below sea level. Iao Valley is the eroded caldera of this dome. Forming an incomplete veneer over the dome are the Honolua soda trachytes and oligoclase andesites. They were extruded in late Pliocene (?) or early Pleistocene time, chiefly from bulbous domes. The clinker beds carry some water but the rocks are generally too dense to be good aquifers. During early (?) Pleistocene the West Maui volcano was cut by deep amphitheater-headed valleys and then all of Maui was deeply submerged.
Four scattered eruptions occurred on West Maui in middle (?) and late Pleistocene time. The cones and lavas cover only small areas and are called the Lahaina volcanic series.
The sedimentary rocks of both East and West Maui are chiefly late Quaternary and comprise fans, landslide debris, delta deposits, and valley fills, mostly of poorly permeable and poorly assorted bouldery alluvium. They are overlain on the Isthmus by extensive calcareous dunes of three ages. A mud flow more than 300 feet thick is exposed in Kaupo Valley. During the fluctuations of the ocean in the Pleistocene, the island was emerged and submerged several times. Calcareous fossiliferous marine conglomerates deposited during this period are found up to an altitude of 250 feet on West Maui.
The Homomanu, Wailuku, and Kula lavas are the chief aquifers. They supply 28 irrigation wells which yield an average of 170 million gallons a day of basal water. These wells are mine-like shafts with infiltration tunnels and are called Maui-type wells. Well 16 yields 40,000,000 gallons daily with a 22-foot drawdown, which is the largest amount yielded by any well in the Hawaiian Islands. The largest spring (no. 26) on the island is artesian. It yields 10,400,000 gallons daily and issues from Kula lavas near Nahiku. West Maui has numerous perennial streams supplied by springs from a dike complex. Twenty-three tunnels in West Maui recover 20.5 million gallons a day of high-level water, mostly from this dike complex. East Maui has few perennial streams in proportion to its size, and they are chiefly small due to the water sheds being underlain with permeable lavas. Forty tunnels recover 6 million gallons a day of high-level water in East Maui and all from structures other than dikes.
It is estimated that about 100 million gallons a day of basal water wastes into the sea from West Maui and about 700 million gallons a day from East Maui. A number of sites are described where wells could be sunk to recover this water. Sites are also described where tunnels could be driven to recover high-level supplies. The hydrology of East and West Maui is conspicuously different in many respects, mainly because of the difference in the stage of dissection, the extensive veneer of very permeable Hann lavas on East Maui, and the comparatively small area of the Lahaina lavas of similar age on West Maui. The only thermal water known in the Hawaiian Islands, except on the active volcano of Kilauea, is in a well in West Maui.
The Nahiku area has been mapped and studied in detail. The upper part of the Honomanu volcanic series, exposed in the sea cliffs, in petrographic character is transitional into the overlying Kula lavas, Kula and Hana time were characterized by a long succession of valley-cutting episodes, each valley being filled by lava erupted from the east rift zone. The lavas include olivine basalts, picritic basalts, and basaltic andesites,
In the Nahiku area basal ground water occurs largely in the Honomanu basalts. Perched water occurs in many of the later lavas, generally following the axes of buried valleys. The members which perch the water are mostly ashy soil beds, although an unusually extensive, thick layer of much decomposed clinker also appears to be a supporting member. Most of the water travels through the basal clinker members of aa lavas. Artesian water is encountered in the upper, transitional part of the Honomanu volcanic series. The aquifer is permeable porphyritic pahoehoe; the confining members are relatively impermeable nonporphyritic aa.
The lavas of East Maui are described according to stratigraphic groups. The oldest or Honomanu lavas are olivine basalts like the primitive lavas in other Hawaiian volcanoes. The later or Kula and Hana lavas include basalts, basaltic andesites, andesites, and picritic basalts. The normative nepheline of analyzed East Maui lavas has not been identified in the mode. The degree of differentiation is inversely proportional to the frequency of eruptions.
The lavas of West Maui volcano are divided into the Wailuku volcanic series, consisting largely of olivine basalts with less abundant olivine-poor basalts, hypersthene basalts, and picritic basalts; the Honolua volcanic series, consisting of oligoclase andesites and soda trachytes; and the Lahaina volcanic series, consisting of nepheline basanite and picritic basalts. Coarse-grained gabbros intrude the Wailuku lavas. Differentiation was undoubtedly partly by crystal settling, but the alkali curves of the variation diagram suggest that volatile transfer was of some importance.
No abstract available.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/b920","usgsCitation":"Bayley, W.S., 1941, Pre-Cambrian geology and mineral resources of the Delaware Water Gap and Easton quadrangles, New Jersey and Pennsylvania: U.S. Geological Survey Bulletin 920, Report: v, 97 p.; 1 Plate: 18.32 × 26.49 inches, https://doi.org/10.3133/b920.","productDescription":"Report: v, 97 p.; 1 Plate: 18.32 × 26.49 inches","costCenters":[],"links":[{"id":397892,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_21096.htm"},{"id":163391,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/0920/report-thumb.jpg"},{"id":92399,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/0920/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":92398,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/0920/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"62500","country":"United States","state":"New Jersey, Pennsylvania","otherGeospatial":"Delaware Water Gap and Easton quadrangles","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -75.25,\n 40.547\n ],\n [\n -75,\n 40.547\n ],\n [\n -75,\n 40.872\n ],\n [\n -75.25,\n 40.872\n ],\n [\n -75.25,\n 40.547\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad2e4b07f02db681b19","contributors":{"authors":[{"text":"Bayley, William Shirley","contributorId":66234,"corporation":false,"usgs":true,"family":"Bayley","given":"William","email":"","middleInitial":"Shirley","affiliations":[],"preferred":false,"id":211910,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":528,"text":"wsp872 - 1941 - Surface water supply of the United States, 1939, Part II, South Atlantic slope and eastern Gulf of Mexico basins","interactions":[],"lastModifiedDate":"2012-02-02T00:05:07","indexId":"wsp872","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1941","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"872","title":"Surface water supply of the United States, 1939, Part II, South Atlantic slope and eastern Gulf of Mexico basins","language":"ENGLISH","publisher":"U.S. Govt. 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Off.,","doi":"10.3133/wsp872","usgsCitation":"Water Resources Division, U.S. Geological Survey, 1941, Surface water supply of the United States, 1939, Part II, South Atlantic slope and eastern Gulf of Mexico basins: U.S. Geological Survey Water Supply Paper 872, ix, 388 p. ;23 cm., https://doi.org/10.3133/wsp872.","productDescription":"ix, 388 p. ;23 cm.","costCenters":[],"links":[{"id":136129,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/0872/report-thumb.jpg"},{"id":25091,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/0872/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afee4b07f02db6974f2","contributors":{"authors":[{"text":"Water Resources Division, U.S. Geological Survey","contributorId":128075,"corporation":true,"usgs":false,"organization":"Water Resources Division, U.S. Geological Survey","id":527500,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":45279,"text":"b899A - 1941 - Geologic structure and occurrence of gas in part of southwestern New York. Part 1, Structure and gas possibilities of the Oriskany sandstone in Steuben, Yates, and parts of the adjacent counties","interactions":[{"subject":{"id":45279,"text":"b899A - 1941 - Geologic structure and occurrence of gas in part of southwestern New York. Part 1, Structure and gas possibilities of the Oriskany sandstone in Steuben, Yates, and parts of the adjacent counties","indexId":"b899A","publicationYear":"1941","noYear":false,"chapter":"A","title":"Geologic structure and occurrence of gas in part of southwestern New York. Part 1, Structure and gas possibilities of the Oriskany sandstone in Steuben, Yates, and parts of the adjacent counties"},"predicate":"IS_PART_OF","object":{"id":33813,"text":"b899 - 1941 - Geologic structure and occurrence of gas in part of southwestern New York","indexId":"b899","publicationYear":"1941","noYear":false,"title":"Geologic structure and occurrence of gas in part of southwestern New York"},"id":1}],"isPartOf":{"id":33813,"text":"b899 - 1941 - Geologic structure and occurrence of gas in part of southwestern New York","indexId":"b899","publicationYear":"1941","noYear":false,"title":"Geologic structure and occurrence of gas in part of southwestern New York"},"lastModifiedDate":"2022-06-13T18:12:17.460206","indexId":"b899A","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1941","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":306,"text":"Bulletin","code":"B","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"899","chapter":"A","title":"Geologic structure and occurrence of gas in part of southwestern New York. Part 1, Structure and gas possibilities of the Oriskany sandstone in Steuben, Yates, and parts of the adjacent counties","docAbstract":"The area covered by this report is in southwestern New York and includes a little more than 3,000 square miles in Steuben and Yates counties and parts of the six adjacent counties. This area has been mapped to determine the structural attitude of the exposed rocks, so as to aid those interested in prospecting for natural gas in the Oriskany sandstone of Lower Devonian age.
Because of the gentle regional dip toward the southwest, the youngest beds are exposed in the southwest corner of the area, and progressively older beds crop out northeastward in successive bands that strike generally northwest. All the exposed rocks are of Upper Devonian age except those in a narrow belt at the extreme north edge of the area, where a small thickness of Middle Devonian rocks crops out. The maximum thickness of beds so exposed is nearly 4,000 feet, of which the lower part is predominantly soft dark shale and the upper part predominantly fine-grained sandstone and gray shale. All the beds are marine except a few tongues of continental deposits red shale and sandstone and gray mudstone in the youngest beds. All the beds thicken southeastward, so that there is a northwestward convergence between any two lithologic units in the series. More than 30 key horizons that are persistent and distinctive were mapped, and altitudes on these key horizons served as a basis for constructing the structure contour map. Many of the key horizons are formation or member boundaries, but others are the tops or bottoms of limestone or sandstone beds within formations. All the stratigraphic units mapped are purely lithologic. (See pi. 2.)
The Tully limestone, which crops out along the northern border of the area, is an easily recognizable and therefore valuable key bed for subsurface correlations in this part of the State. Below the Tully limestone is a thick body of Middle Devonian shales of the Hamilton group which rests on another valuable key bed, the hard, cherty Onondaga limestone, also of Middle Devonian age. Below the Onondaga limestone is the Lower Devonian Oriskany sandstone, which is the gas-producing bed. Unlike the Onondaga, the Oriskany is locally thin or absent.
The structure of most of the area is shown by contour lines at 25-foot intervals, but where key horizons are lacking the structure is indicated by dip symbols. Upon the regional south and southwest dip are superposed numerous gentle folds whose axes trend approximately northeastward in the greater part of the area but more nearly eastward in the eastern part. The folds generally tend to become narrower and steeper, and therefore more closely spaced, southwestward. Many of the anticlines fork southwestward, whereas the synclines. tend to fork northeastward. All the folds have a westward or southwestward plunge.
Throughout the area the rocks are jointed in two dominant sets one that trends northwest and the other east or northeast. No evident relation .between these joints, which were measured only in the hard, relatively brittle beds, and the individual folds or domes was discernible.
The faults are concentrated in the northeastern and southwestern parts of the area and trend either northeastward or northwestward. Some are nearly vertical normal faults; others are steep reverse faults. Subsurface data show that most of the faults increase in throw downward and also that many subsurface faults do not reach the surface. A group of faults in the northwestern part of the Greenwood quadrangle and the southwestern part of the Hornell quadrangle were active during Upper Devonian time, while the Gowanda shale and overlying beds were being deposited. At this stratigraphic horizon the beds in a zone a few hundred feet thick are highly deformed in a wide belt on both sides of the faults. Sandstone layers are thinned out into long stringers or swollen into thick masses and in places are bent acutely without fracture. Thin layers of shale, coquina, and sand have flowed together into intricately plicated zones that lack cleavage and joints. These features show that the sediments were deformed while wet and plastic and buried only a little way below the sea floor. The beds that were laid down over these disturbed zones were not involved in this deformation. Many of the sharper flexures and most of the faults are not evident in the beds several hundred feet stratigraphically higher. Accordingly, broad, gentle folds in these higher beds in parts of the area south and west of the northwest corner of the Greenwood quadrangle may conceal, at considerable depths below them, narrow folds separated by abrupt flexures or faults.
Several of the larger streams and rivers occupy strike valleys, and their j courses swing to follow the changing strike of the rocks where they cross ( successive folds. But, with few exceptions, the small streams are not adjusted to the bedrock structure.
Domes likely to serve as traps for natural gas are concentrated in the northeastern and southwestern parts of the area. The Wayne-Dundee gas field is in the northeastern part. All the other potentially valuable domes in this part of the area have been drilled and found valueless except one small structural feature in the southern part of the Ovid quadrangle, which, if the Oriskany is present, may trap a small quantity of gas.
In the Greenwood quadrangle in the southwestern part of the area there is one gas field and four well-defined domes, all of which may be productive if the Oriskany sandstone is present. In the northwest corner of the quadrangle the dips indicate at least two domes that can be adequately defined and evaluated only by geophysical prospecting. The State Line gas field is in tbe Wellsville quadrangle. In the southeast corner of this quadrangle there are three other domes of comparable size that may also be productive if underlain by the Oriskany sandstone. At other places in the Wellsville quadrangle the dips suggest several anticlinal axes on which analogous productive domes maybe found. The structural features in this quadrangle, however, are defined by contours only in the southeastern part. In the Woodhull quadrangle a large dome east of Jasper may be productive, and the western top of the large Woodhull dome in the southwestern part of the quadrangle seems to warrant drilling, despite the absence of the Oriskany in a well on the eastern top. Two wells drilled in 1936 and 1937 a little northeast of a broad, nearly flat-topped dome in the Hornell quadrangle, a few miles east of Hornell,, struck small flows of gas, suggesting that wells drilled higher on this dome may be productive.
In much of the southwestern part of the area seismograph surveys should be of great value in determining the structure at the Tully and Onondaga horizons. Without abundant subsurface control of this sort, the danger of drilling into subsurface faults can hardly be overemphasized.
Three closed or nearly closed synclines in the Greenwood and Wellsville quadrangles appear to be favorable places to drill for oil in the shallow sands presumably parts of the Dunkirk sandstone.
","language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/b899A","usgsCitation":"Bradley, W.H., and Pepper, J.F., 1941, Geologic structure and occurrence of gas in part of southwestern New York. Part 1, Structure and gas possibilities of the Oriskany sandstone in Steuben, Yates, and parts of the adjacent counties: U.S. Geological Survey Bulletin 899, Report: iii, 68 p.; 1 Plate: 33.98 x 35.11 inches, https://doi.org/10.3133/b899A.","productDescription":"Report: iii, 68 p.; 1 Plate: 33.98 x 35.11 inches","costCenters":[],"links":[{"id":93910,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/0899a/plate-2.pdf","text":"Plate 2","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 2"},{"id":402106,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_93211.htm"},{"id":134603,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/0899a/report-thumb.jpg"},{"id":93911,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/0899a/report.pdf","text":"Report","linkFileType":{"id":1,"text":"pdf"},"description":"Report"}],"country":"United States","state":"New York","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -78,\n 43\n ],\n [\n -78,\n 42\n ],\n [\n -76.75,\n 42\n ],\n [\n -76.75,\n 43\n ],\n [\n -78,\n 43\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ae0e4b07f02db68817c","contributors":{"authors":[{"text":"Bradley, W. H.","contributorId":102452,"corporation":false,"usgs":true,"family":"Bradley","given":"W.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":231345,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Pepper, J. F.","contributorId":71522,"corporation":false,"usgs":true,"family":"Pepper","given":"J.","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":231344,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":45287,"text":"b900G - 1941 - Subsurface geology and oil and gas resources of Osage County, Oklahoma. Part 7, Townships 20 and 21 north, ranges 11 and 12 east","interactions":[{"subject":{"id":45287,"text":"b900G - 1941 - Subsurface geology and oil and gas resources of Osage County, Oklahoma. Part 7, Townships 20 and 21 north, ranges 11 and 12 east","indexId":"b900G","publicationYear":"1941","noYear":false,"chapter":"G","title":"Subsurface geology and oil and gas resources of Osage County, Oklahoma. Part 7, Townships 20 and 21 north, ranges 11 and 12 east"},"predicate":"IS_PART_OF","object":{"id":33723,"text":"b900 - 1942 - Subsurface geology and oil and gas resources of Osage county, Oklahoma","indexId":"b900","publicationYear":"1942","noYear":false,"title":"Subsurface geology and oil and gas resources of Osage county, Oklahoma"},"id":1}],"isPartOf":{"id":33723,"text":"b900 - 1942 - Subsurface geology and oil and gas resources of Osage county, Oklahoma","indexId":"b900","publicationYear":"1942","noYear":false,"title":"Subsurface geology and oil and gas resources of Osage county, Oklahoma"},"lastModifiedDate":"2021-08-30T22:33:33.079774","indexId":"b900G","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1941","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":306,"text":"Bulletin","code":"B","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"900","chapter":"G","title":"Subsurface geology and oil and gas resources of Osage County, Oklahoma. Part 7, Townships 20 and 21 north, ranges 11 and 12 east","docAbstract":"No abstract available.
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Part 8, Parts of township 20 north, ranges 9 and 10 east, and township 21 north, ranges 8 and 9 east and all of township 21 north, range 10 east","indexId":"b900H","publicationYear":"1941","noYear":false,"chapter":"H","title":"Subsurface geology and oil and gas resources of Osage County, Oklahoma. Part 8, Parts of township 20 north, ranges 9 and 10 east, and township 21 north, ranges 8 and 9 east and all of township 21 north, range 10 east"},"predicate":"IS_PART_OF","object":{"id":33723,"text":"b900 - 1942 - Subsurface geology and oil and gas resources of Osage county, Oklahoma","indexId":"b900","publicationYear":"1942","noYear":false,"title":"Subsurface geology and oil and gas resources of Osage county, Oklahoma"},"id":1}],"isPartOf":{"id":33723,"text":"b900 - 1942 - Subsurface geology and oil and gas resources of Osage county, Oklahoma","indexId":"b900","publicationYear":"1942","noYear":false,"title":"Subsurface geology and oil and gas resources of Osage county, Oklahoma"},"lastModifiedDate":"2022-04-28T18:50:30.576715","indexId":"b900H","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1941","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":306,"text":"Bulletin","code":"B","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"900","chapter":"H","title":"Subsurface geology and oil and gas resources of Osage County, Oklahoma. Part 8, Parts of township 20 north, ranges 9 and 10 east, and township 21 north, ranges 8 and 9 east and all of township 21 north, range 10 east","docAbstract":"The area whose subsurface geology and oil and gas resources are described in this report lies along the southern border of Osage County, Okla., and includes parts of T. 20 N., Rs. 9 and 10 E., and of T. 21 N., Rs. 8 and 9 E., and all of T. 21 N., R. 10 E. The towns of Osage and Prue are within the area; Cleveland, which is a mile south of the Arkansas River, is not far beyond its southwestern limit; and Tulsa is 10 miles east of its southeast corner. The production of oil and gas from the many fields in the five townships began as early as 1905, and drilling has continued up to the present. Oil or gas is produced from 13 zones at depths ranging from 250 to 2,600 feet. Of these zones, one is in the Ordovician system, one is at the contact of the Mississippian and the Pennsylvanian series, and all others are in the Pennsylvanian series. The five townships lie within a region that contains many oil and gas fields in the Bartlesville sand; the Red Fork sand is oil-bearing in a narrow belt in T. 21 N., R. 8 E.; and oil and gas are produced in small areas from the Taneha, Skinner, Squirrel, Cleveland, Jones, and Layton sands, the Mussehem and Peoples sand zone, the Okesa, Torpedo, and Clem Creek sand zone, and the Big lime and Peru sand zone.
The rocks dip westward across the five townships at an average rate of about 38 feet to the mile as measured on the top of the Oswego lime. This regional dip is interrupted, however, by many anticlines, domes, synclines, and structural basins. The subsurface crests of most of the domes and anticlines are not directly under the crests as determined on the exposed rocks, and the dips of the deeper rocks are steeper and the structural closures greater in the buried rocks than in the exposed rocks. The exposed rocks are cut by several faults that trend northwest, but the data are insufficient to determine whether the deeply buried rocks, also, are displaced along the faults.
This investigation has shown that there are a few localities not yet completely tested in this part of Osage County that may produce oil and gas and that a few producing oil fields have areas within or adjacent to them that have not been thoroughly prospected. It is pointed out that yields of oil and gas from limy reservoir rocks may be increased by acid treatment and that additional oil may be produced from some of the reservoir sands by repressuring them with gas or flooding them with water.
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B.","contributorId":50867,"corporation":false,"usgs":true,"family":"Goodrich","given":"H.","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":231382,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70206706,"text":"70206706 - 1941 - Geology of the Moreno Valley, New Mexico","interactions":[],"lastModifiedDate":"2019-11-18T12:58:33","indexId":"70206706","displayToPublicDate":"1941-12-31T12:51:22","publicationYear":"1941","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1786,"text":"Geological Society of America Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Geology of the Moreno Valley, New Mexico","docAbstract":"The Moreno Valley, located along the complex eastern boundary between the Sangre de Cristo Mountains and the Great Plains, is structurally a broad, northwardplunging syncline, disrupted by smaller folds and faults. This major synclinal structure is the result of the Laramide disturbance. Deformation, however, has continued possibly into the Quaternary. Intrusions, probably contemporaneous with those of the Spanish Peaks, have deformed the strata in the northern portion of the Moreno Valley. Scully Mountain is a northwestward-plunging anticline produced by a porphyry intrusion. A Mid-Tertiary surface of low relief is now represented by broad mountain flats at elevations near 10,000 feet. The Moreno Valley was initiated as a topographic feature about the close of the Mid-Tertiary. Its subsequent history is in many respects similar to that of the Rio Grande Depression. During the Quaternary a broad valley stage and three lower pediments have been developed. The lowest pediments are cut on deformed valley fill, believed to be Pliocene and here named the Eagle Nest formation. The early drainage of the valley was south and east into the Canadian River. Stream piracy by the Cimarron River diverted drainage to the east through the present Cimarron Canyon into the Canadian River. Drainage south of the point of capture has been reversed for about 14 miles, the present stream draining the southern portion of the Moreno Valley flowing northward to the Cimarron River. © 1941 Geological Society of America.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/GSAB-52-177","issn":"00167606","usgsCitation":"Ray, L., and Smith , J., 1941, Geology of the Moreno Valley, New Mexico: Geological Society of America Bulletin, v. 52, no. 2, p. 177-210, https://doi.org/10.1130/GSAB-52-177.","productDescription":"34 p. ","startPage":"177","endPage":"210","costCenters":[],"links":[{"id":369289,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"New Mexico ","county":"Colfax County ","otherGeospatial":"Moreno Valley ","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-105.2198,36.9961],[-105.1432,36.9958],[-105.1011,36.9957],[-105.066,36.9954],[-105.0326,36.9934],[-104.3313,36.993],[-104.1849,36.9958],[-104.0068,36.9966],[-104.0067,36.4374],[-104.009,36.218],[-104.4368,36.2193],[-104.6433,36.2177],[-104.6701,36.2176],[-104.7049,36.2175],[-104.7363,36.2178],[-104.7762,36.2187],[-104.8646,36.2177],[-104.8651,36.2617],[-105.2428,36.2629],[-105.2862,36.2627],[-105.3683,36.2627],[-105.3599,36.2694],[-105.3484,36.2714],[-105.3432,36.2704],[-105.3388,36.2697],[-105.3357,36.2709],[-105.3355,36.2712],[-105.3325,36.272],[-105.332,36.2748],[-105.3267,36.2768],[-105.3355,36.3011],[-105.3353,36.3224],[-105.3335,36.3333],[-105.3282,36.3442],[-105.3294,36.3487],[-105.3294,36.3496],[-105.3299,36.3519],[-105.3299,36.3542],[-105.3287,36.3587],[-105.3304,36.3632],[-105.3309,36.3669],[-105.3309,36.3682],[-105.336,36.3692],[-105.3354,36.3714],[-105.3308,36.3764],[-105.3285,36.38],[-105.3267,36.39],[-105.3267,36.3913],[-105.3267,36.3941],[-105.3266,36.399],[-105.3289,36.404],[-105.3294,36.4077],[-105.3322,36.4113],[-105.3413,36.4155],[-105.3401,36.4245],[-105.3412,36.4331],[-105.3389,36.439],[-105.3428,36.4468],[-105.3479,36.4504],[-105.3473,36.4577],[-105.3455,36.464],[-105.3437,36.4681],[-105.3414,36.4726],[-105.3402,36.4794],[-105.3373,36.4826],[-105.3316,36.487],[-105.3252,36.4893],[-105.3224,36.4924],[-105.3269,36.4952],[-105.3303,36.4993],[-105.3354,36.5057],[-105.3365,36.5084],[-105.3468,36.5121],[-105.3479,36.5171],[-105.349,36.5252],[-105.3506,36.5289],[-105.3535,36.5316],[-105.3592,36.5389],[-105.3614,36.5403],[-105.3706,36.5453],[-105.3762,36.5531],[-105.3768,36.554],[-105.3756,36.5558],[-105.3613,36.557],[-105.3509,36.5624],[-105.3509,36.567],[-105.352,36.5742],[-105.3525,36.5792],[-105.3542,36.5856],[-105.357,36.5892],[-105.3638,36.5979],[-105.3695,36.602],[-105.3718,36.607],[-105.3711,36.6152],[-105.3688,36.6201],[-105.3647,36.6242],[-105.3601,36.6273],[-105.3572,36.6282],[-105.3549,36.6305],[-105.3538,36.6341],[-105.3514,36.6391],[-105.3548,36.6432],[-105.3577,36.6477],[-105.3605,36.6518],[-105.3645,36.6582],[-105.3627,36.6645],[-105.3661,36.67],[-105.3683,36.6741],[-105.3677,36.6804],[-105.3608,36.6872],[-105.3532,36.6958],[-105.3446,36.6966],[-105.3348,36.7025],[-105.3274,36.6988],[-105.3233,36.6997],[-105.3186,36.711],[-105.3139,36.7241],[-105.3065,36.725],[-105.2875,36.7258],[-105.2813,36.7198],[-105.2744,36.7198],[-105.2669,36.717],[-105.2577,36.7174],[-105.252,36.7129],[-105.2492,36.7129],[-105.2428,36.7228],[-105.2393,36.7223],[-105.2365,36.7223],[-105.2347,36.7223],[-105.2336,36.7227],[-105.2318,36.7232],[-105.2313,36.7241],[-105.2301,36.7259],[-105.2249,36.7313],[-105.2249,36.7327],[-105.2254,36.7372],[-105.2253,36.7431],[-105.2235,36.7494],[-105.2241,36.7508],[-105.2246,36.7599],[-105.2268,36.7635],[-105.2279,36.7712],[-105.229,36.7771],[-105.2329,36.7935],[-105.2264,36.8016],[-105.227,36.8039],[-105.2316,36.8066],[-105.2321,36.8107],[-105.228,36.8148],[-105.228,36.8215],[-105.2239,36.8233],[-105.2233,36.8292],[-105.2244,36.836],[-105.2289,36.8406],[-105.23,36.8479],[-105.2276,36.8601],[-105.2218,36.865],[-105.2194,36.875],[-105.2176,36.8768],[-105.2165,36.8777],[-105.2129,36.8922],[-105.2052,36.9044],[-105.2052,36.9076],[-105.2121,36.9135],[-105.2137,36.9203],[-105.2223,36.9249],[-105.2205,36.9303],[-105.2227,36.9426],[-105.2266,36.9553],[-105.2352,36.9626],[-105.2345,36.9712],[-105.2402,36.9762],[-105.2361,36.9798],[-105.2361,36.9835],[-105.232,36.9871],[-105.2205,36.9911],[-105.2198,36.9961]]]},\"properties\":{\"name\":\"Colfax\",\"state\":\"NM\"}}]}","volume":"52","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Ray, L.L.","contributorId":73741,"corporation":false,"usgs":true,"family":"Ray","given":"L.L.","email":"","affiliations":[],"preferred":false,"id":775492,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Smith , J.F. Jr. ","contributorId":220707,"corporation":false,"usgs":false,"family":"Smith ","given":"J.F. ","suffix":"Jr. ","affiliations":[],"preferred":false,"id":775493,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70213276,"text":"70213276 - 1941 - Depth of active solution by ground‐waters in the Pecos Valley, New Mexico","interactions":[],"lastModifiedDate":"2020-09-16T19:44:23.733022","indexId":"70213276","displayToPublicDate":"1941-09-16T14:32:40","publicationYear":"1941","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1578,"text":"Eos, Transactions, American Geophysical Union","onlineIssn":"2324-9250","printIssn":"0096-394","active":true,"publicationSubtype":{"id":10}},"title":"Depth of active solution by ground‐waters in the Pecos Valley, New Mexico","docAbstract":"The Pecos River Drainage‐Basin is underlain by a thick series of Permian rocks consisting largely of limestone, gypsum (or anhydrite), and halite. The beds have a regional eastward or southeastward dip of 40 to 80 feet to the mile and successively younger beds are exposed at the surface from west to east across the Basin (Fig, 1). The beds of the San Andres formation and the Chalk Bluff formation or its equivalents crop out over most of the broad western part of the Basin (Fig. 1). Most of the eastern part of the Basin is immediately underlain by the redbeds was sandstone of the Dockum group, of Triassic age, which, south of Acme, are separated from the Chalk Bluff formation by the Salado and Rustler formations. North of Acme the Dockum group overlaps successively older formations ana northwest of Santa Rosa it rests upon beds in the lower part of the San Andres formation.
","language":"English","publisher":"American Geophysical Union","doi":"10.1029/TR022i003p00779","usgsCitation":"Morgan, A., 1941, Depth of active solution by ground‐waters in the Pecos Valley, New Mexico: Eos, Transactions, American Geophysical Union, v. 22, no. 3, p. 779-783, https://doi.org/10.1029/TR022i003p00779.","productDescription":"5 p.","startPage":"779","endPage":"783","costCenters":[],"links":[{"id":378470,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"New Mexico","otherGeospatial":"Pecos River Drainage Basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -106.10595703125,\n 36.54494944148322\n ],\n [\n -106.23779296875,\n 35.60371874069731\n ],\n [\n -106.36962890624999,\n 34.52466147177172\n ],\n [\n -106.3916015625,\n 32.82421110161336\n ],\n [\n -106.23779296875,\n 32.0639555946604\n ],\n [\n -103.33740234375,\n 32.045332838858506\n ],\n [\n -103.18359375,\n 36.87962060502676\n ],\n [\n -106.06201171875,\n 36.914764288955936\n ],\n [\n -106.10595703125,\n 36.54494944148322\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"22","issue":"3","noUsgsAuthors":false,"publicationDate":"2014-08-18","publicationStatus":"PW","contributors":{"authors":[{"text":"Morgan, Arthur M.","contributorId":59051,"corporation":false,"usgs":true,"family":"Morgan","given":"Arthur M.","affiliations":[],"preferred":false,"id":798933,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70213269,"text":"70213269 - 1941 - Factors influencing runoff during the flood of December, 1937, in northern California","interactions":[],"lastModifiedDate":"2020-09-17T13:50:56.499789","indexId":"70213269","displayToPublicDate":"1941-09-16T12:28:00","publicationYear":"1941","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1578,"text":"Eos, Transactions, American Geophysical Union","onlineIssn":"2324-9250","printIssn":"0096-394","active":true,"publicationSubtype":{"id":10}},"title":"Factors influencing runoff during the flood of December, 1937, in northern California","docAbstract":"Engineers and hydrologists engaged on flood‐problems throughout much of the United States east of the Rocky Mountains must deal to a considerable extent with wide‐spread storms covering thousands of square miles. The gradations of meteorologic conditions as regard both area and time are relatively homogeneous during such storm‐events and are affected but moderately by orographical influences. Under such conditions similar storm‐characteristics prevail over vast areas. True, precipitation decreases toward the boundaries of such major storm‐areas, and locally precipitation‐rates may greatly exceed the average. Often, however, drainage‐basin after drainage‐basin will yield comparable depths of flood‐runoff. The storms of March, 1936, which resulted in the simultaneous occurrence of floods throughout all of the northeastern part of the United States from Ohio and Virginia to Maine and the storm of January, 1937, which embraced all of the 200,000 square miles comprising the Ohio River drainage are typical of major Eastern disturbances. The storm of December, 1937, in the Sacramento and San Joaquin valleys is used herein to illustrate what may be called a typical major California disturbance, and it is this storm and resulting flood that I wish to consider in some detail and also to make such comparisons and contrasts with Eastern floods as seem to be of general interest.
","language":"English","publisher":"American Geophysical Union","doi":"10.1029/TR022i001p00124","usgsCitation":"Boyt, W., 1941, Factors influencing runoff during the flood of December, 1937, in northern California: Eos, Transactions, American Geophysical Union, v. 22, no. 1, p. 124-129, https://doi.org/10.1029/TR022i001p00124.","productDescription":"6 p.","startPage":"124","endPage":"129","costCenters":[],"links":[{"id":378461,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -124.134521484375,\n 37.47485808497102\n ],\n [\n -120.498046875,\n 37.47485808497102\n ],\n [\n -120.498046875,\n 40.18726672309203\n ],\n [\n -124.134521484375,\n 40.18726672309203\n ],\n [\n -124.134521484375,\n 37.47485808497102\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"22","issue":"1","noUsgsAuthors":false,"publicationDate":"2014-08-18","publicationStatus":"PW","contributors":{"authors":[{"text":"Boyt, W.G.","contributorId":240765,"corporation":false,"usgs":false,"family":"Boyt","given":"W.G.","email":"","affiliations":[],"preferred":false,"id":798924,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70213267,"text":"70213267 - 1941 - Magnetic studies by the Geophysical Section of the United States Geological Survey","interactions":[],"lastModifiedDate":"2020-09-16T17:05:51.805795","indexId":"70213267","displayToPublicDate":"1941-09-16T11:57:32","publicationYear":"1941","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1578,"text":"Eos, Transactions, American Geophysical Union","onlineIssn":"2324-9250","printIssn":"0096-394","active":true,"publicationSubtype":{"id":10}},"title":"Magnetic studies by the Geophysical Section of the United States Geological Survey","docAbstract":"Continued progress has been made in magnetic surveys over large sectional areas by G. R. MacCarthy. Beginning in Florida south of the Okeefenokee Swamp, magnetic traverses were measured and continued through the southern part of Georgia. The most northerly traverses crossed regions where they contacted the crystallines near the surface of the ground. All traverses were run in an east‐west direction. It is planned to continue the magnetic relief‐map described in the Transactions of 1939 of the American Geophysical Union by adding to it this portion of the State of Georgia.
","language":"English","publisher":"American Geophysical Union","doi":"10.1029/TR022i002p00460","usgsCitation":"Lee, F., 1941, Magnetic studies by the Geophysical Section of the United States Geological Survey: Eos, Transactions, American Geophysical Union, v. 22, no. 2, p. 460-462, https://doi.org/10.1029/TR022i002p00460.","productDescription":"3 p.","startPage":"460","endPage":"462","costCenters":[],"links":[{"id":378454,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"22","issue":"2","noUsgsAuthors":false,"publicationDate":"2014-08-18","publicationStatus":"PW","contributors":{"authors":[{"text":"Lee, F.W.","contributorId":240764,"corporation":false,"usgs":false,"family":"Lee","given":"F.W.","email":"","affiliations":[],"preferred":false,"id":798922,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":57109,"text":"ofr4132 - 1941 - Contamination of Lake Wewoka and fresh-water sands by disposal of oil-well brines near Wewoka, Seminole County, Oklahoma","interactions":[],"lastModifiedDate":"2024-02-28T19:48:14.361805","indexId":"ofr4132","displayToPublicDate":"1941-01-01T00:00:00","publicationYear":"1941","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"41-32","title":"Contamination of Lake Wewoka and fresh-water sands by disposal of oil-well brines near Wewoka, Seminole County, Oklahoma","docAbstract":"This report deals with ground-water conditions in an area about 5 miles wide from east to west and 8 miles long from north to south, in Tps. 8 and 9 N., Rs. 7 and 8 E., in Seminole County, Oklahoma, including the town of Wewoka and Lake Wewoka. The possible contamination of the lake waters from oil-well brines disposed through a well 3.75 miles north of the lake, and other effects of brine disposal, are considered.
The investigation was made at the request of Frank Raab, member of the Oklahoma Planning and Resources Board, and Don McBride, Chief Engineer of the Division of Water Resources who has the responsibility of preventing contamination of water supplies in Oklahoma.
Field work was done July 5 and 6, 1941, by Robert H. Dott, Director of the Oklahoma Geological Survey; C.G. Lalicker, Department of Geology, University of Oklahoma; and S.L. Schoff, Assistant Geologist in the Ground Water Division, Water Resources Branch, of the U.S. Geological Survey.
Lalicker spent both days studying the rocks exposed in the vicinity and measuring their thickness. A copy of the composite section measured by him is attached. Dott and Schoff spent one day collecting the well information summarized in Table 1, and one day with Lalicker on the stratigraphy.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr4132","collaboration":"Prepared in cooperation with the Oklahoma Geological Survey","usgsCitation":"Schoff, S., Dott, R.H., and Lalicker, C.G., 1941, Contamination of Lake Wewoka and fresh-water sands by disposal of oil-well brines near Wewoka, Seminole County, Oklahoma: U.S. Geological Survey Open-File Report 41-32, 10 p., https://doi.org/10.3133/ofr4132.","productDescription":"10 p.","costCenters":[],"links":[{"id":425377,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1941/0032/report-thumb.jpg"},{"id":426083,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1941/0032/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Oklahoma","county":"Seminole County","city":"Wewoka","otherGeospatial":"Lake Wewoka","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -96.53713981428714,\n 35.2310650782901\n ],\n [\n -96.53713981428714,\n 35.100794501825334\n ],\n [\n -96.43448923082433,\n 35.100794501825334\n ],\n [\n -96.43448923082433,\n 35.2310650782901\n ],\n [\n -96.53713981428714,\n 35.2310650782901\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afde4b07f02db696bd4","contributors":{"authors":[{"text":"Schoff, Stuart L.","contributorId":104467,"corporation":false,"usgs":true,"family":"Schoff","given":"Stuart L.","affiliations":[],"preferred":false,"id":511599,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Dott, Robert H.","contributorId":87620,"corporation":false,"usgs":true,"family":"Dott","given":"Robert","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":511598,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Lalicker, Cecil Gordon","contributorId":69233,"corporation":false,"usgs":true,"family":"Lalicker","given":"Cecil","email":"","middleInitial":"Gordon","affiliations":[],"preferred":false,"id":511597,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":33813,"text":"b899 - 1941 - Geologic structure and occurrence of gas in part of southwestern New York","interactions":[{"subject":{"id":45279,"text":"b899A - 1941 - Geologic structure and occurrence of gas in part of southwestern New York. Part 1, Structure and gas possibilities of the Oriskany sandstone in Steuben, Yates, and parts of the adjacent counties","indexId":"b899A","publicationYear":"1941","noYear":false,"chapter":"A","title":"Geologic structure and occurrence of gas in part of southwestern New York. Part 1, Structure and gas possibilities of the Oriskany sandstone in Steuben, Yates, and parts of the adjacent counties"},"predicate":"IS_PART_OF","object":{"id":33813,"text":"b899 - 1941 - Geologic structure and occurrence of gas in part of southwestern New York","indexId":"b899","publicationYear":"1941","noYear":false,"title":"Geologic structure and occurrence of gas in part of southwestern New York"},"id":1},{"subject":{"id":45280,"text":"b899B - 1941 - Geologic structure and occurrence of gas in part of southwestern New York. Part 2. Subsurface structure in part of southwestern New York and mode of occurrence of gas in the Medina group","indexId":"b899B","publicationYear":"1941","noYear":false,"chapter":"B","title":"Geologic structure and occurrence of gas in part of southwestern New York. Part 2. Subsurface structure in part of southwestern New York and mode of occurrence of gas in the Medina group"},"predicate":"IS_PART_OF","object":{"id":33813,"text":"b899 - 1941 - Geologic structure and occurrence of gas in part of southwestern New York","indexId":"b899","publicationYear":"1941","noYear":false,"title":"Geologic structure and occurrence of gas in part of southwestern New York"},"id":2}],"lastModifiedDate":"2017-03-08T09:29:16","indexId":"b899","displayToPublicDate":"1938-01-01T11:10:00","publicationYear":"1941","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":306,"text":"Bulletin","code":"B","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"899","title":"Geologic structure and occurrence of gas in part of southwestern New York","docAbstract":"The area covered by this report is in southwestern New York and includes a little more than 3,000 square miles in Steuben and Yates counties and parts of the six adjacent counties. This area has been mapped to determine the structural attitude of the exposed rocks, so as to aid those interested in prospecting for natural gas in the Oriskany sandstone of Lower Devonian age.
Because of the gentle regional dip toward the southwest, the youngest beds are exposed in the southwest corner of the area, and progressively older beds crop out northeastward in successive bands that strike generally northwest. All the exposed rocks are of Upper Devonian age except those in a narrow belt at the extreme north edge of the area, where a small thickness of Middle Devonian rocks crops out. The maximum thickness of beds so exposed is nearly 4,000 feet, of which the lower part is predominantly soft dark shale and the upper part predominantly fine-grained sandstone and gray shale. All the beds are marine except a few tongues of continental deposits—red shale and sandstone and gray mudstone—in the youngest beds. All the beds thicken southeastward, so that there is a northwestward convergence between any two lithologic units in the series. More than 30 key horizons that are persistent and distinctive were mapped, and altitudes on these key horizons served as a basis for constructing the structure contour map. Many of the key horizons are formation or member boundaries, but others are the tops or bottoms of limestone or sandstone beds within formations. All the stratigraphic units mapped are purely lithologic. (See pl. 2.)
The Tully limestone, which crops out along the northern border of the area, is an easily recognizable and therefore valuable key bed for subsurface correlations in this part of the State. Below the Tully limestone is a thick body of Middle Devonian shales of the Hamilton group which rests on another valuable key bed, the hard, cherty Onondaga limestone, also of Middle Devonian age. Below the Onondaga limestone is the Lower Devonian Oriskany sandstone, which is the gas-producing bed. Unlike the Onondaga, the Oriskany is locally thin or absent.
The structure of most of the area is shown by contour lines at 25-foot intervals, but, where key horizons are lacking the structure is indicated by dip symbols. Upon the regional south and southwest dip are superposed numerous gentle folds whose axes trend approximately northeastward in the greater part of the area but more nearly eastward in the eastern part. The folds generally tend to become narrower and steeper, and therefore more closely spaced, southwestward. Many of the anticlines fork southwestward, whereas the synclines tend to fork northeastward. All the folds have a westward or southwestward plunge.
Throughout the area the rocks are jointed in two dominant sets—one that trends northwest and the other east or northeast. No evident relation between these joints, which were measured only in the hard, relatively brittle beds, and the individual folds or domes was discernible.
The faults are concentrated in the northeastern and southwestern parts of the area and trend either northeastward or northwestward. Some are nearly vertical normal faults ; others are steep reverse faults. Subsurface data show that most of the faults increase in throw downward and also that many subsurface faults do not reach the surface. A group of faults in the northwestern part of the Greenwood quadrangle and the southwestern part of the Hornell quadrangle were active during Upper Devonian time, while the Gowanda shale and overlying beds were being deposited. At this stratigraphic horizon the beds in a zone a few hundred feet thick are highly deformed in a wide belt on both sides of the faults. Sandstone layers are thinned out into long stringers or swollen into thick masses and in places are bent acutely without fracture. Thin layers of shale, coquina, and sand have flowed together into intricately plicated zones that lack cleavage and joints. These features show that the sediments were deformed while wet and plastic and buried only a little way below the sea floor. The beds that were laid down over these disturbed zones were not involved in this deformation. Many of the sharper flexures and most of the faults are not evident in the beds several hundred feet stratigraphically higher. Accordingly, broad, gentle folds in these higher beds in parts of the area south and west of the northwest corner of the Greenwood quadrangle may conceal, at considerable depths below them, narrow folds separated by abrupt flexures or faults.
Several of the larger streams and rivers occupy strike valleys, and their courses swing to follow the changing strike of the rocks where they cross successive folds. But, with few exceptions, the small streams are not adjusted to the bedrock structure.
Domes likely to serve as traps for natural gas are concentrated in the northeastern and southwestern parts of the area. The Wayne-Dundee gas field is in the northeastern part. All the other potentially valuable domes in this part of the area have been drilled and found valueless except one small structural feature in the southern part of the Ovid quadrangle, which, if the Oriskany is present, may trap a small quantity of gas.
In the Greenwood quadrangle in the southwestern part of the area there is one gas field and four well-defined domes, all of which may be productive if the Oriskany sandstone is present. In the northwest corner of the quadrangle the dips indicate at least two domes that can be adequately defined and evaluated only by geophysical prospecting. The State Line gas field is in the Wellsville quadrangle. In the southeast corner of this quadrangle there are three other domes of comparable size that may also be productive if underlain by the Oriskany sandstone. At other places in the Wellsville quadrangle the dips suggest several anticlinal axes on which analogous productive domes may be found. The structural features in this quadrangle, however, are defined by contours only in the southeastern part. In the Woodhull quadrangle a large dome east of Jasper may be productive, and the western top of the large Wood-hull dome in the southwestern part of the quadrangle seems to warrant drilling, despite the absence of the Oriskany in a well on the eastern top. Two wells drilled in 1936 and 1937 a little northeast of a broad, nearly flat-topped dome in the Hornell quadrangle, a few miles east of Hornell, struck small flows of gas, suggesting that wells drilled higher on this dome may be productive.
In much of the southwestern part of the area seismograph surveys should be of great value in determining the structure at the Tully and Onondaga horizons. Without abundant subsurface control of this sort, the danger of drilling into subsurface faults can hardly be overemphasized.
Three closed or nearly closed synclines in the Greenwood and Wellsville quadrangles appear to be favorable places to drill for oil in the shallow sands— presumably parts of the Dunkirk sandstone.
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The basic period for which the computations are made is the water year or year ending September 30. \r\n\r\nAs it is impractical to present in this report all the basic data used in arriving at the results, only sample computations are given. The various steps in the computations and the probable accuracy of the results are discussed. The drainage areas for which data are presented are those above river-measuring stations that have records for 3 years or more. For each area there are determinations of annual rainfall, annual run-off, and annual water loss for each year of record .as well as the means for the period of record. Results are given for about 200 drainage areas with an aggregate period of record of more than 2,000 years. As an illustration of the magnitude involved, the annual water loss from the eastern streams draining directly into the Atlantic Ocean varies more or less closely with latitude from about 20 inches as an average in northern New England to about 30 inches in Georgia. \r\n\r\nAs the annual water loss from a basin is affected by the temperature, a supplemental study was made of the relation between water loss and temperature. For 28 drainage areas selected in various parts 8f eastern and central United States, average temperatures were computed for each year of the period shown in table 1. The results indicate a relation between average annual water loss and average annual temperature.","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp846","usgsCitation":"Williams, G.R., 1940, Natural water loss in selected drainage basins: U.S. Geological Survey Water Supply Paper 846, iv, 62 p. :ill., map ;24 cm., https://doi.org/10.3133/wsp846.","productDescription":"iv, 62 p. :ill., map ;24 cm.","costCenters":[],"links":[{"id":139445,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/0846/report-thumb.jpg"},{"id":29760,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/0846/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0ae4b07f02db5fba7f","contributors":{"authors":[{"text":"Williams, Gordon R.","contributorId":51729,"corporation":false,"usgs":true,"family":"Williams","given":"Gordon","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":146109,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":518,"text":"wsp852 - 1940 - Surface water supply of the United States, 1938, Part II, South Atlantic slope and eastern Gulf of Mexico basins","interactions":[],"lastModifiedDate":"2012-02-02T00:05:08","indexId":"wsp852","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1940","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"852","title":"Surface water supply of the United States, 1938, Part II, South Atlantic slope and eastern Gulf of Mexico basins","language":"ENGLISH","publisher":"U.S. Govt. 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Off.,","doi":"10.3133/wsp852","usgsCitation":"Water Resources Division, U.S. Geological Survey, 1940, Surface water supply of the United States, 1938, Part II, South Atlantic slope and eastern Gulf of Mexico basins: U.S. Geological Survey Water Supply Paper 852, vi, 293 p. ;23 cm., https://doi.org/10.3133/wsp852.","productDescription":"vi, 293 p. ;23 cm.","costCenters":[],"links":[{"id":136139,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/0852/report-thumb.jpg"},{"id":25081,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/0852/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afee4b07f02db697550","contributors":{"authors":[{"text":"Water Resources Division, U.S. Geological Survey","contributorId":128075,"corporation":true,"usgs":false,"organization":"Water Resources Division, U.S. Geological Survey","id":527490,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":45284,"text":"b900D - 1940 - Subsurface geology and oil and gas resources of Osage County, Oklahoma. Part 4, Townships 24 and 25 north, ranges 10 and 11 east","interactions":[{"subject":{"id":45284,"text":"b900D - 1940 - Subsurface geology and oil and gas resources of Osage County, Oklahoma. Part 4, Townships 24 and 25 north, ranges 10 and 11 east","indexId":"b900D","publicationYear":"1940","noYear":false,"chapter":"D","title":"Subsurface geology and oil and gas resources of Osage County, Oklahoma. Part 4, Townships 24 and 25 north, ranges 10 and 11 east"},"predicate":"IS_PART_OF","object":{"id":33723,"text":"b900 - 1942 - Subsurface geology and oil and gas resources of Osage county, Oklahoma","indexId":"b900","publicationYear":"1942","noYear":false,"title":"Subsurface geology and oil and gas resources of Osage county, Oklahoma"},"id":1}],"isPartOf":{"id":33723,"text":"b900 - 1942 - Subsurface geology and oil and gas resources of Osage county, Oklahoma","indexId":"b900","publicationYear":"1942","noYear":false,"title":"Subsurface geology and oil and gas resources of Osage county, Oklahoma"},"lastModifiedDate":"2021-08-30T22:30:19.972605","indexId":"b900D","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1940","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":306,"text":"Bulletin","code":"B","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"900","chapter":"D","title":"Subsurface geology and oil and gas resources of Osage County, Oklahoma. 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Part 2, South-central Missouri, 1908-37","interactions":[{"subject":{"id":45260,"text":"b916B - 1940 - Transit traverse in Missouri, 1900-1937. Part 2, South-central Missouri, 1908-37","indexId":"b916B","publicationYear":"1940","noYear":false,"chapter":"B","title":"Transit traverse in Missouri, 1900-1937. 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South-central Missouri, as the term is used in this bulletin and as the subject of part 2 of the bulletin, is that section of the State lying south of latittude, 38°00' and between longitudes 91°15' and 93°00'.
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East-central Missouri, as the term is used in this bulletin and as the subject of part 3 of the bulletin, is that section of the State lying between latitudes 38°00' and 39°15' and east of longitude 92°00'.
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Northwestern Missouri, as the term is used in this bulletin and as the subject of part 4 of the bulletin, is that section of the State lying north of latitude 39°30' and west of longitude 93°15'
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Part 5, Southwestern Missouri, 1900-37","interactions":[{"subject":{"id":45263,"text":"b916E - 1940 - Transit traverse in Missouri, 1900-1937. Part 5, Southwestern Missouri, 1900-37","indexId":"b916E","publicationYear":"1940","noYear":false,"chapter":"E","title":"Transit traverse in Missouri, 1900-1937. 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Southwestern Missouri, as the term is used in this bulletin and as the subject of part 5 of the bulletin, is that section of the State lying south of latitude 38°00' and west of longitude 93°00'.
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Northeastern Missouri, as the term is used in this bulletin and as the subject of part 6 of the bulletin, is, as its name indicates, the north-easternmost section of the State. Its north and east boundaries are the boundaries of the State; its west and south boundaries are formed by a line that runs south along longitude 93°15' to latitude 39°30', thence east to longitude 92°00', thence south to latitude 39°15', thence east to the east boundary of the State.
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Central Missouri, as the term is used in this bulletin and as the subject of part 7 of the bulletin, is that section of the State lying between latitudes 36°00' and 39°30' and between longitudes 92°00' and 93°30'.
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West-central Missouri, as the term is used in this bulletin and as the subject of part 8 of the bulletin, is that section of the State lying between latitudes 38°00' and 39°30' and west of longitude 93°30'.
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