RIVER ROUGE

city, adjacent to southwest Detroit, Wayne county, Michigan, U.S.. It lies along the Detroit and Rouge rivers. The site of an early French settlement, it grew in the 1920s with the development of the Ford Motor Company's plant in nearby Dearborn. Available rail and water transportation encouraged industrialization; the city's manufactures now include paper, ships, gypsum products, and steel. Zug Island, a highly industrialized 400-acre (162-hectare) site formed by a canal dredged between the two rivers, is in the city's northeast corner. Inc. village, 1889; city, 1921. Pop. (1993 est.) 11,274. Streamflow and sediment yield Peak discharge and flooding Rapid variations of water-surface level in river channels through time, in combination with the occurrence from time to time of overbank flow in flat-bottomed valleys, have promoted intensive study of the discharge relationships and the probability characteristics of peak flow. Stage (depth or height of flow) measurements treat water level: discharge measurements require determinations of velocity through the cross section. Although records of stage respond to frequency analysis, the analysis of magnitude and frequency is preferable wherever stage is affected by progressive scour or fill, and also where channels have been artificially embanked or enlarged or both. The velocity determinations needed to calculate discharge range from those obtained with portable Venturi flumes on very small streams, through observations with gaging staff or fixed Venturi flumes on streams of modest size, to soundings with current meters at intervals of width and depth at cross sections of large rivers. Frequent velocity observations on large rivers are impracticable. It is standard practice to establish a rating formula, expressed graphically by a rating curve. Such a curve relates height of water surface to the area of and velocity through the cross section and thus to discharge. Secular changes in rating occur where a stream tends progressively to raise or lower its bed elevation. Short-term changes are common where the bed is mobile and especially where the bed elevationdischarge relation, and thus the stagedischarge relation, differs between the rising and the falling limb of a single peak discharge curve. In such cases the rating curve describes a hysteresis loop. Rating curves for sand-bed streams can include discontinuities, chiefly during rising discharge, that relate to behavioral jumps on the part of the bed. Floods in hydrology are any peak discharges, regardless of whether or not the valley floor (if present) is inundated. The timedischarge or timestage characteristics of a given flood peak are graphed in the hydrograph, which tends to assume a set form for a given station in response to a given input of water. The peak flow produced by a single storm is superimposed on the base flow, the water already in the channel and being supplied from the groundwater reservoir. Rise to peak discharge is relatively swift and is absolutely swift in small basins and on torrents where the duration of the momentary peak is also short. On very large streams, by contrast, peak discharge can be sustained for lengths of days. Recession from peak discharge is usually exponential. The form of the hydrograph for any one station is affected by characteristics of the channel and the drainage net, as well as by basin geometry, all of which can be taken as permanent in this context. As noted above, flood-flow prediction that is based on permanent characteristics has hitherto achieved but partial success. Transient influences, also highly and at times overwhelmingly important, include the storage capacity of bedrock and soil, the interrelationships of infiltration, evaporation, and interception and detention (especially by vegetation), plus storm characteristics, which vary widely with respect to amount, duration, intensity, and location of rainfall with respect to the catchment. In the longer term, flood-frequency analysis based on recorded past events can nevertheless supply useful predictions of future probabilities and risks. Flood-frequency analysis deals with the incidence of peak discharges, whereas frequency analysis generally provides the statistical basis of hydraulic geometry. Percentage frequency analysis has been much used in engineering: here, the 1 percent and 90 percent discharges, for instance, are those that are equalled or exceeded 1 and 90 percent of time, respectively. General observations of the flashy character of floods in headwater streams, in contrast to the long durations of flood waves far downstream, combine with analytical studies to suggest, however, that percentage frequency is in some respects an unsuitable measure. Magnitudefrequency analysis, setting discharge against time, is directly applicable in studies of hydraulic geometry and flood-probability forecasting. Regional graphs of magnitudefrequency can be developed, given adequate records, for floods of any desired frequency or magnitude. Predictions for great magnitudes and low frequencies, however, demand records longer than those usually available. Twelve years of record are needed to define the mean annual flood within 25 percent, with an expectation of correct results for 95 percent of time; and in general, a record should be at least twice as long as the greatest recurrence interval for which magnitude is desired. Predictions of overbank flow, whether or not affected by artificial works, are relevant to floodplain risk and floodplain management. Notably in the conterminous United States, floodplain zoning is causing risks to be reduced by the withdrawal of installations from the most flood-liable portions of floodplains or risks to be totally accepted by occupiers. In the long geomorphic term the transmission of sediment through floodplain storage systems and through stream channels seems to result mainly from the operation of processes of modest magnitude and high frequency. Specifically, analyses suggest that total sediment transport by rivers is normally affected by flows approximating bank-full over durations ranging down from 25 to 1 percent of total time. Infrequent discharges of great magnitude, which can be expected on grounds of the probabilities of precipitation, snowmelt, and streamflow, range widely in destructive effect. Severe flooding is normally accompanied by great loss of life and property damage, the mean annual floods along the Huang Ho themselves affecting some 29,800 square kilometres of floodplain, but geomorphic effects may be minimal, even with very large floods. The approximately 100-year floods of eastern England in the spring of 1947, fed by unusually great and deferred snowmelt, scarcely affected either channels or floodplains. The 1955 floods in Connecticut, fed by rains amounting to 58 centimetres in places, produced only spotty effects of erosion and deposition, even where floodplains were inundated to a depth of six metres. For a given valley, there could be a threshold of inundation, river velocity, and sediment load, beyond which drastic changes occur. This is suggested, for example, by the catastrophic alluviation of valleys in eastern Australia and New Zealand during the last 4,000 or 2,000 years. Sudden catastrophes in historical and geomorphic records are related to special events, mainly nonrecurrent: the 1841 Indus flood, which destroyed an army; the Gohna Lake flood of 1894 on the Ganges; and the 1925 Gros Ventre flood in Wyoming, accompanied the breaching of natural landslide barriers. The Lake Issyk-Kul (Kyrgyzstan) flood of 1963, which caused widespread erosion and deposition, followed the overtopping of a landslide barrier by waves produced by a mudflow. The Vaiont Dam (Italy), although itself holding, was overtopped in 1963 by 91-metre-high waves raised by a landslide: the floods downstream took more than 2,500 lives in 15 minutes. On the Huang Ho the floods of 1887 took an estimated 900,000 lives. In late Pleistocene time the overtopping of an erodible natural dam by the then-existing Lake Bonneville eventually released nearly 1,666 cubic kilometres of water; the maximum discharge of about 280,000 cubic metres per second is comparable to the flow of the Amazon, but velocities were very high, perhaps ranging to 7.6 metres per second. The greatest flood peak so far identified is that of the ice-dammed Lake Missoula in Montana, which, on release, discharged 2,085 cubic kilometres of water at an estimated peak flow of 8,500,000 cubic metres per second. Iceland is notable for glacier bursts, which are nonrecurrent where they result from subglacial eruptions but recurrent where they involve the sudden failure of ice dams, as with Grmsvtn, which periodically releases 8.3 or more cubic kilometres of water in floods that peak at 57,000 cubic metres per second. Deposition by glacier-burst floods is illustrated by Iceland's Sandur plains. Peak discharges that close the range between natural floods of great magnitude and low frequency on noncatastrophic streams and natural catastrophic floods of great magnitude and perceptible frequency include stormwater discharges from expanding urban areas. Because of the progressive spread of impermeable catchment and efficient runoff systems, such floods tend to increase both in frequency and in magnitude. George Harry Dury The Editors of the Encyclopdia Britannica Sediment yield and sediment load All of the water that reaches a stream and its tributaries carries sediment eroded from the entire area drained by it. The total amount of erosional debris exported from such a drainage basin is its sediment yield. Sediment yield is generally expressed in two ways: either as a volume or as a weighti.e., as acre-feet (one-foot depth of material over one acre) or as tons. In order to adjust for the very different sizes of drainage basins, the yield frequently is expressed as a volume or weight per unit area of drainage basine.g., as acre-feet per square mile or as tons per square mile or per square kilometre. The conversion between the two forms of expression is made by obtaining an average weight for the sediment and calculating the total weight from the measured volume of sediment. Further, sediment yield is usually measured during a period of years, and the results are thus expressed as an annual average. The sediment delivered to and transported by a stream is its sediment load. This can be classified into three types, depending on sediment size and the competence of the river. The coarsest sediment, consisting of boulders and cobbles as well as sand, moves on or near the bed of the stream and is the bed load of the river. The finer particles, silts and clays, are carried in suspension by the turbulent action of flowing water; and these fine particles, which are moved long distances at the velocity of the flowing water, constitute the suspended load of the river. The remaining component of the total sediment load is the dissolved load, which is composed of chemical compounds taken into solution by the water moving on or in the soils of the drainage basin. These three types of sediment constitute the total sediment load of the stream and, of course, the sediment yield of the drainage basin.