Calcareous Sandy Research Articles

Kaibab Limestone and Associated Strata, Circle Cliffs , Utah

Exposed Permian rocks studied in the Circle Oiffs region are the upper part of the White Rim Sandstone Formation of the Cutler Group and the overlying Kaibab Limestone. The former is composed of calcareous and dolomitic sandstones and sandy dolomites formed under stable tectonic conditions in a nearshore marine environment by reworking of the underlying aeolian portion of the White Rim Member. The Kaibab Limestone is actually a slightly calcareous, partly sandy, glauconitic dolomite which was chiefly a biomicrite before dolomitization. It formed in shallow, though quiet, marine waters under tectonically quiescent conditions. It disconformably overlies the White Rim Sandstone. Detrital intertidal and very shallow subtidal sediments of the lowermost Moenkopi Formation (Triassic), mostly chert breccias, overlie the irregular, partly channeled surface of the Kaibab Limestone. This ' attests to post-Kaibab emergence and erosion. Uniformity of lithologies and thicknesses of individual Permian beds traced across the Circle Cliffs Anticline demonstrate the absence of a late Permian paleostructure.

Nitrogen balance studies for different Egyptian soils cropped with corn

The nitrogen balance for four different Egyptian soils cropped with corn and fertilized with increasing amounts of ammonium sulphate was studied in pot experiments. The tested soils were clay loam, calcareous sandy loam, sandy loam and sand. Nitrogen added as seeds, fertilizers, irrigation water and insecticides, nitrogen removed by the plants including thinned plants and fallen leaves and the nitrogen content of the soils before sowing and after the harvest were determined and used to draw the balance sheet.

Radiocarbon dated shell samples from Nordre Strømfjord, West Greenland, with comments on models of glacio-isostatic uplift

Shell-bearing marine sediments in the Nordre Strømfjord area belong to two lithofacies, calcareous sandy gravels and calcareous muddy sands, and to four biofacies comparable to modem communities and related to the sediment lithology: epifaunal benthic and infaunal benthic facies, a current reworked 'mixed' facies and a Portlandia - Propeamussium fades. Radiocarbon dates on nine samples provide a poorly defined model of the glacio-isostatic emergence of the region. The implications of such models and their physical validity are considered in the context of these and other data, and it is suggested that curves for uplift deceleration are a useful means of obtaining the exponential constant k.

Effects of nitrogen fertilizer, plant population and irrigation on sugar beet: I. Yields

SUMMARYFive experiments (1965–9) on calcareous sandy loam tested all combinations of four amounts of nitrogen (0–1·8 cwt/acre N) and four plant populations (8000–54 000 plants/ acre) given to sugar beet grown with and without irrigation. On average, nitrogen and plant population influenced yields greatly but irrigation relatively little. In all years between 0·6 and 1·2 cwt/acre N and between 17000 and 32000 plants/acre gave largest sugar yield. Giving more nitrogen or increasing the plant population neither increased nor decreased sugar yield much in any year. Irrigation was beneficial in only two out of five years.Sugar yield was linearly related to root dry-matter yield. Although total dry matter was greatest when the largest plant population was given the largest dressing of nitrogen and irrigation, the proportion of dry matter in the roots was decreased by all three factors.

Effectiveness of Zn Frits for Corn (Zea mays L.) as Influenced by Zn Concentration, Granule Size and Method of Application1

AbstractA greenhouse experiment was conducted to study the influence of Zn concentration, particle size, and methods of application on the effectiveness of Zn frit‐concentrated superphosphate (CSP) mixtures3 in relation to ZnSO4. Two crops of sweet corn (Zea mays L.) were grown on a neutral loamy sand soil and a calcareous sandy loam soil. The effect of Zn concentration and particle size of the Zn frits on the solubility of these materials in water and in an acid solution was studied.Zinc frits mixed with CSP were as effective as ZnSO4 on a neutral soil, but tended to be less effective than ZnSO4 on a calcareous soil. Effectiveness of granular Zn frit‐CSP mixtures decreased as the concentration of Zn increased, and the fine material was more effective than the granular material at the 12% Zn concentration on the calcareous soil. In the laboratory study no difference in solubility was found between the fine and granular 12% Zn frit carriers. Therefore, it was concluded that the reduced effectiveness of the 12% granular Zn frit was due to fewer particles and reduced surface area rather than to decreased solubility.

Response of ‘Valencia’ Orange Trees to Four Soil Water Schedules During 20 Years1

Abstract ‘Valencia’ orange scions on sour orange rootstock, planted in 1935 at Tempe, Arizona, in calcareous sandy loam, were grown from 1949 through 1968 under 4 irrigation programs: high—15 irrigations a year, 1.72 m water applied; moderate—10 irrigations a year, 1.35 m water applied; low—5 irrigations a year, 0.95 m water applied; high-low—high, March to July, and low, August to February, 9 irrigations a year, 1.18 m water applied. Yields were similar in high, moderate and high-low trees; reduced in low trees. Trunk growth was proportionately reduced as less water was applied. High soil water produced larger tree canopies than moderate, low and high-low, which were similar. Summer shoot growth was stimulated in high trees, limited by fruiting and soil water deficits in moderate and high-low regimes, and promoted by reduced yields in low trees. Low soil water reduced total feeder roots and increased the proportion below 60 cm. Fruit sizes were similar in high and moderate, markedly reduced in high-low and variable in low schedules. Total soluble solids in fruit increased as less water was applied after mid-July. Peel thickness was similar in high and moderate and thinner than in low and high-low. High yields from the high-low regime show there is no advantage in maintaining high soil water during the entire year. Moderate stresses after July induced highest soluble solids in fruit, maintained smaller trees which facilitated picking, and prevented iron chlorosis.

The effect of intermittent drying and wetting of a calcareous soil on carbon and nitrogen mineralization

The mineralization of carbon and nitrogen in a calcareous sandy loam soil with and without the addition of lucerne meal and incubated continuously for 12 weeks, was compared with the mineralization of carbon and nitrogen in similar soils dried and rewetted every two weeks. The amount of carbon and nitrogen mineralized and the total number of micro-organisms were determined periodically.

Morphology and Genesis of Some Soils Containing Fragipans in Northern Michigan

AbstractDetailed physical, chemical, and mineralogical studies were made on profiles representative of the McBride, Isabella, and Nester series. These are soils that were formed in calcareous sandy loam, sandy clay loam, and clay loam tills, respectively, in northern Michigan. They are bisequal profiles representative of the zonal Podzol group, intergrading to Gray Wooded soils. They each contain eluvial fragipan horizons (Eq) between the overlying illuvial humus sesquioxide horizon (Ihi) and the underlying illuvial silicate clay or textural horizon (It). Genesis of the Podzol sequum is characterized by high physical, chemical, and biological activities, while the underlying Gray Wooded sequum is characterized mainly by leaching of soluble materials and high physical activity such as eluviation, illuviation, contraction, and rearrangements of soil particles.The fragipan is most strongly developed in the McBride. The fragipans occur at depths of 8 to 20 inches beneath the surface and are 6 to 24 inches thick. They are deeper and thicker in the soils formed in the moderately coarsetextured primary materials. The fragipans are grayer and more compact than adjoining layers. They have high bulk densities, are hard when dry and firm when moist. When moist, the resistance of the materials studied to the penetration of a metal cone increases with clay contents up to about 15%. With higher clay contents their resistance decreases rapidly. The clay in these horizons is largely illitic but some chlorite and kaolinite are also present. The clay and silt form a dense matrix or bridges between the sand grains.The alterations of the primary materials necessary for the formation of the pedogenetic fragipan horizons include: leaching of lime, eluviation of the finer expanding lattice clays leaving a residual concentration of the coarser nonexpanding clay, compaction of the layers by weight of the overlying layers or the tap roots of plants, and possibly some weak reversible cementation with soluble alumina.The fragipan layers interfere with the movement of water and plant roots in the soil profile. Roots branch little in these layers and tap roots of alfalfa commonly zigzag through cracks in them.

Palaeozoic and Mesozoic Formations in the Vicinity of Fukumoto, Okayama Prefecture : A Study on the Stratigraphy and the Geologic Structure of the "Maizuru Zone" (Part 1)

The Upper Permian Kose group, the Lower and Middle Triassic Fukumoto group, the Upper Triassic Yanagi formation and Nakaiso conglomerate beds, the so-called Inkstone group, and basic intrusive rocks crop out in the vicinity of Fukumoto-mura in Okayama Prefecture., The Palaeozoic and Mesozoic formations in this district, together with the basic rocks, indicate that the Zone extends into Okayama Prefecture about 130km., WSW of Maizuru in Kyoto Prefecture., The stratigraphy of the Palaeozoic and Triassic formations is shown in the following table., Norian?-Nakaiso conglomerate beds., ., ., ., ., ., mainly conglomerate with sandstone, thickness 200m., unconformity? Carnian-Yanagi formation., ., ., ., ., ., black shale and carbonaceous sandy shale, thickness 70m., fault Anisian-Miyano-oku formation., ., ., ., ., ., dark blue calcareous sandy shale with shale and fine sandstone, thickness 300m., Kyogakubo formation., ., ., ., ., ., alternation of shale and sandstone, thickness 270-300m., Scythian -Kusano formation., ., ., ., ., ., mainly fine to medium sandstone with conglomerate, thickness 68-96m+., fault Upper Permian-Kose group., ., ., ., ., ., mainly black shale with sandstone and conglomerate lens, thickness 350m -., The Kose group contains fusulinids such as Lepidolina, sp., and Yabeina, sp., and is correlated with the Upper Permian Kuma series in Kyushu., The Fukumoto group contains pelecypod-fossils such as Neobakevellia kanb i NAKAZAWA (MS., ), Myophoria, aff., laevigata, ALBERTI, Eumorphotis sp., nov, and Pecten sichoticus BITTNER, in the Kusano and Kyogakubo formations, and cephalopods such as Hollandites sp., Danubites sp., and Orthoceras sp., in the Miyano-oku formation., From these fossils the group is considered Scythian and Anisian in age., The group is in fault contact with the Kose group, but is supposed to overlie the Kose group unconformably., The Norian (?) Nakaiso conglomerate beds overlie the Kose and Fukumoto groups in angular unconformity as a result of a severe crustal movement of Ladinian or Carnian age.,

Marine Jurassic Formations of Sweetgrass Arch, Montana

The marine Jurassic rocks of the Sweetgrass arch in western north-central Montana have been assigned to the Ellis formation. As a result of measuring and sampling eleven Jurassic sections around the Sweetgrass arch and from examining numerous well cuttings, the writer concludes that the Ellis consists of three major lithologic divisions that should be recognized as formations, and that the Ellis should be raised to group rank. The formations of the Ellis group from oldest to youngest are herein named Sawtooth, Rierdon, and Swift. The Sawtooth formation consists of three members, a basal fine-grained sandstone, a medial dark gray shale containing a few dark limestone beds, and an upper member of light gray calcareous siltstone, fine-grained sandstone, or sandy, oolitic limestone. The Sawtooth is as little as 8 feet in thickness on the Kevin-Sunburst dome. It thickens eastward to 200 feet in the Sweetgrass Hills and westward to about 200 feet along the Rocky Mountain Front. The formation is absent over most of the South arch. The lower two members pass into redbeds east of the Sweetgrass Hills and on the southeast flank of the South arch. The Rierdon formation consists mainly of gray limy shale and nodular limestone. It seems to overlie the Sawtooth formation conformably. It is as little as 72 feet in thickness on the Kevin-Sunburst dome, but thickens eastward to 180 feet in the Sweetgrass Hills and westward to about 200 feet along the Rocky Mountain Front. The formation is absent over most of the South arch. The Swift formation is composed of two members along the Rocky Mountain Front and eastward across the Kevin-Sunburst dome at least as far as the Sweetgrass Hills. The lower member is dark non-calcareous shale, highly glauconitic at the base. The upper member is gray fine-grained flaggy glauconitic sandstone containing abundant black-gray micaceous shale partings. On the South arch the formation consists of fine-grained flaggy sandstone which is locally pebbly at the base. In the vicinity of the Little Belt Mountains the formation is massive fine-grained sandstone containing a prominent basal conglomerate. The Swift attains its maximum thickness of 166 feet in the Pondera field. The formation has been removed by pre-Kootenai erosion from most of the Cut Bank area, and from a small area west of the Whitlash field. All the formations are fossiliferous. According to Imlay, the Sawtooth is upper Bathonian, the Rierdon is upper Bathonian and Callovian, and the Swift is Divesian and Argovian. The South arch was an island through most of the Bathonian and Callovian stages. At the close of the Callovian the marine waters retreated from the area. During the early Divesian the Sawtooth and Rierdon formations were locally thinned by erosion and possibly removed from some areas. Later in the Divesian marine waters transgressed the entire area and remained until the close of the Argovian.