Long-term effects expressed in mean seasonal regimes and short-term effects expressed in individual peak flows are alike affected by soil-moisture conditions, groundwater balance, and channel storage. Channeled surface flow begins when overland flow becomes deep enough to be erosive; and depth of overland flow represents a balance between short-term precipitation and soil infiltration. Rate and capacity of infiltration depend partly on antecedent conditions and partly on permeability. Seasonal assessments are possible, however; numbers of commercial crops can take up and transpire the equivalent of 38 centimetres of precipitation during the growing season. In many midlatitude climates the rising curves of insolation and plant growth during spring and early summer cause soil moisture depletion, leading eventually to a deficit that is often strong enough to reduce runoff and streamflow. Soil moisture recharge during colder months promotes high values of runoff frequently in the spring quite independently of the influence of precipitation regime or snowmelt.

Storage of water in groundwater tables, in stream channels, on floodplains, and in lakes damps out variations in flow, whereas snow and ice storage exaggerate peaks. For the world as a whole, groundwater contributes perhaps 30 percent of total runoff, although the proportion varies widely from basin to basin, within basins, and through time. Shallow groundwater tables in contact with river channels absorb and release water, respectively at high and low stage. Percolation to greater depths and eventual discharge through springs delays the entry of water into channels; many groundwater reservoirs carry over some storage from one year to another. Similar carryover occurs with glaciers and to some extent also with permanent snowfields; water abstracted by the ice caps of high latitudes and by large mountain glaciers can be retained for many years, up to about 250,000 years in the central Antarctic cap. Temperate glaciers, however, with temperatures beneath the immediate subsurface constantly near the freezing (or the melting) point, can, like their associated snowfields, release large quantities of water during a given warm season. Their losses through evaporation are small.

Meltwater contributions to streamflow, however, can range from well above half the total discharge to well below the level of the snow line. They are vital to irrigation on alluvial fans rimming many dry basins, as in the Central Valley of California and the Tarim Basin of the Takla Makan Desert of China: meltwater is released during the planting or growing seasons. Within the limiting constraints of precipitation or meltwater input or both, and the outputs of evapotranspiration and percolation, the actual distribution of rivers in nature is affected by available drainage area, lithology, and vegetation. Vegetation is obviously climate dependent to a large extent but might well be capable of reaching thresholds of detention ability that do not match recognized climatic boundaries. It is, moreover, liable to the influence of climatically independent factors where it has been disturbed by human activity. Runoff on the plain lands of northern Asia, expressed as a percentage of mean annual precipitation, ranges from about 75 in the tundra, through about 70 in the boreal forest and 50 through boreal forest with perennially frozen ground, down through less than 40 in mixed forest, to five in semidesert. Clear felling of forest increases runoff in the short and medium term because it reduces surface detention and transpiration. In areas of seasonal snow cover, forest influences seasonal regime considerably. However, though there may be a jump in short-term runoff characteristics between areas of continuous vegetation (forest and grass sward) on the one hand and discontinuous vegetation (bunchgrass and scrub) on the other, comprehensive general studies of precipitation-temperature runoff characteristics suggest that mean annual runoff decreases, at a decreasing rate through the range that is involved, as temperature increases and as precipitation (weighted in respect of seasonal incidence) decreases.

Lithology is significant mainly in connection with permeability. The capacity of karst to swallow and to reissue water is well known, as is the role of permeable strata generally in absorbing water into groundwater tables. An extreme case of a special kind is represented by an artesian aquifer, which in favourable structural conditions can take water for a very long time from the surface and immediately connected circulations, returning it only if the artesian pressure becomes strong enough to promote the opening of flowing springs. Less directly, but with considerable effect on infiltration and short-term runoff, the mechanical grade of bedrock or of surficial deposits can considerably affect the response to individual storms.

Both the ultimate possible extent of drainage basins and the opening of individual headwater channels are influenced by available drainage area. A hypothetical limit for very large basins could probably be constructed from considerations of stem length, basin shape, computed area, and continental extent. The Amazon probably approaches the hypothetical maximum. At the other extreme, basin morphometry (geometric aspects of basins and their measurement) can be made to indicate the limiting average area necessary to sustain a given length of channel; in large areas of the midlatitudes, the ratio is close to 2.25 square kilometres of drainage area for a channel 1.6 kilometres in length. Estimates for the conterminous United States, an area of about 7,770,000 square kilometres, give some 5,230,000 kilometres of channel length. These estimates include 1,500,000 unbranched fingertip tributaries—each having an average length of 1.6 to 2.4 kilometres.