The characteristics of a river and its valley found in this course include vertical erosion, lakes, waterfalls, potholes, rapids and gorges. Overland flow is found in depressions making lakes. Eventually, the channel gets deeper and waterfalls become rapids.
Characteristics include, lateral erosion, transportation, floodplain, meanders, truncated spurs, and river cliffs. The gradient of the river is increasingly even and smooth, and the flood plain begins to develop.
Here, transportation and deposition are found. The channel is large and features such as Deltas, levees, bluffs and meanders are found. The flood plain increases in size as meanders migrate downstream.
The drainage basin - as stated earlier - is an example of an open system, and many of the terms above are central to it. Below is a flow diagram of the drainage basin system:
All rivers receive a water supply and the area of land this comes from is known as a drainage basin. The boundaries of the basin are known as the watershed and will usually be marked by areas of higher land.
Drainage basins have many different characteristics that influence how quickly or slowly the main river within them responds to a period of intense rainfall, these are outlined in more detail in the section relating to storm hydrographs.
This relates to the number of streams in a particular drainage basin and can be measured by dividing total length of all streams in a basin (L) by its area (A). As a rule, the higher the drainage density (D) the more quickly water drains to a river.
D = total L/A
Characteristics of high and low-density drainage basins:
High density (+2km per km2)
Impermeable land surface, steep slopes, limited vegetation cover, limited rainfall, gentle slopes, large channel frequency (tributaries).
(-2km per km)
Permeable rock, for example, chalk, much vegetation cover, limited rainfall, gentle sloes, lower channel frequency.
As with drainage density, this allows for quantitative study of drainage basins and therefore comparison between different basins. A.N. Strahler, who states that there is a relationship between stream order and number, developed stream ordering. The basic idea is shown in the diagram below:
First order streams: original, single source tributaries.
Second-order streams: the joining of two first order streams.
Third order streams: the merging of two-second order streams.
Streams of different order may join together for example a second and third order stream. The order given is that of the highest order stream. An entire drainage basin is named after the highest order stream found within it, for example, a fourth order drainage basin.
Relationships are also found between:
stream order and the number of stream in a drainage basin (negative correlation).
stream length and stream order (positive correlation).
area of drainage basin and stream order (positive correlation).
It is assumed that the results are plotted on semi-log paper. The ideal relationships found between stream order and number of streams is shown in the graphs below:
Storm hydrographs are graphs that show how a drainage basin responds to a period of rainfall. They are useful in planning for flood situations and times of drought as they show the discharge (amount of water reaching channel via surface run-off, throughflow, and base flow) that originated as precipitation.
Drainage basins all have a variety of characteristics in terms of vegetation, geology, soil type and so on, all of which interact to influence how quickly or slowly river discharge increases after a storm. The table below outlines the major influences on hydrographs and drainage basins:
Size of basin, shape and relief
Size - the smaller the basin the less time it takes for water to drain to the river, resulting in a shorter lag time. Shape - the shape of basin that lends itself to most rapid drainage is circular. In a long, narrow basin water takes longer to reach the river. Relief - the steeper the basin the more quickly it drains.
Forms of precipitation
Heavy Storms - in such a situation, rainfall is often far in excess of the infiltration capacity of the soil leading to much overland flow, and rapid rises in river levels. Lengthy rainfall - leads to the ground being saturated and overland flow. Snowfall - until snow melts, potential discharge for a river is held in storage. Rapid melting can lead to flooding.
High rates of evapotranspiration reduce amounts of discharge, and low temperatures can store water in the form of ice and snow.
Vegetation - Important in reducing discharge as it intercepts precipitation and adds to rates of evapotranspiration. Roots of plants take up water reducing throughflow. Interception is less in winter in the UK due the shedding of leaves from deciduous trees. Flooding is more likely in deforested areas.
Rock type varies within drainage basins and can be permeable (allowing water through) or impermeable (not allowing water through). Permeable rocks can be porous such as chalk that store water within them or pervious, such as limestone where water flows along bedding plains. Impermeable rocks encourage grater amounts of surface run-off and a more rapid increase in discharge than permeable rocks.
A control on the rate of infiltration, amount of soil moisture storage and rate of throughflow. Larger pore spaces as found in sand, allow for greater water storage and limit the risk of flooding.
As stated earlier, the higher the density the greater the risk of flooding.
Tides and storms
High spring tides (illustrated by the Severn Bore) prevent water from entering the sea and increase the risk of flooding.
A major impact because of its alteration on the hydrological process. The main affects are shown on the diagram below. Click on the magnifying glass to see the graph in more detail.
Recharge: Replacement of water lost during drier periods.
The maximum amount of water soil can hold.
A water surplus can result in wet soils, high river levels and run-off whereas a deficit leads to dry soil, falling river levels and possibly drought. Management is shown in the example at the end of this topic.
Evapotranspiration is in excess of precipitation and any previously available moisture has been used, in soil moisture utilisation.
The regime of a river is expected to have a seasonal pattern of discharge during the year. This is due to factors such as climate, local geology and human interaction. Equatorial rivers have regular regimes but in the UK where seasons exist one or two peaks may be recognisable.
If a river has more than one period of high water levels and/or low water levels, a more complex regime results. It is more common on large rivers that flow through a variety of relief and receive their water supply from large tributaries, for example, The Rhine.
A river has two main functions: one, to transport water and two, to transport sediment. The type of flow that occurs depends on factors such as gradient, volume of water, channel shape, and friction.
There are two types of flow:
Laminar Flow: This rarely occurs, water flows smoothly in a straight channel. It is most common in the lower parts of a river. It is shown in the diagram below:
Turbulent flow: This is far more common, it occurs where the shape of the rivers channel is varied with pools, meanders, and rapids. A great deal of turbulence results in sediment being disturbed. The greater the velocity the larger the quantity and size of particles that can be transported. Turbulent flow is illustrated in the diagram below:
It is often thought that the velocity of a river is greatest near its start. This is not the case, as large angular boulders create a rough channel shape and therefore, a large amount of its bed friction. This creates more resistance to flow than a river with smooth clays and silt forming its banks. The roughness coefficient is measured using Manning's 'n', which shows the relationship between channel roughness and velocity. The equation is as follows:
A long answer that you will need to plan, and should spend approximately half an hour answering. Careful consideration of the ways processes interact to result in a high or low probability of flooding is vital. Figures and reference to a storm event should be used to support your answer.
Begin with a brief outline of the main characteristics of your drainage basin:
"The drainage basin of the River X is located in... It has an elongated shape, and the relief is predominantly low lying. The climate is mild with winter temperatures rarely falling below freezing."
Reference to the following is required:
Basin size / shape / relief
Land use and vegetation (farming, forestry etc.)
Any urban areas
Rock and soil type
How these factors influence the processes of infiltration, evapotranspiration, soil moisture stores etc.
For example: " Discharge for the river is highest from October to January when numerous depressions pass over the area. Evapotranspiration is reduced at this time as a result of low temperatures and limited interception a result of leaf loss from deciduous trees. These factors combine to increase the flood risk at this time of the year. An example of this was shown in..."
(Marks available: 15)
a) What are the chief processes operating in a drainage basin system?
b) How can change to land use in a river channel limit flooding? You should include references to a named river.
This describes the process whereby water in its various forms is continually cycled between the land, sea and atmosphere. It also makes its way into the biosphere to influence animal and plant ecosystems around the globe.
This is a common approach in geography and the two main examples in this topic are:
The hydrological cycle: a closed system.
The drainage basin system: an open system.
Both consist of transfers, stores, inputs of water but the hydrological cycle is a closed system as no gains or losses from outside are added to the system.
The drainage basin system is said to be open as both inputs and outputs of energy and material occur. All systems in their natural state aim to be in a state of balance (dynamic equilibrium) as this is when they function best. Heavy rainfall, drought and human activity such as deforestation can easily upset the balance.
Within the hydrological cycle, four main processes operate:
This is when plants prevent some rainfall from directly reaching the ground, for example, water on leaves or foliage. It may later reach the floor via stem flow (water flows down the stem to the ground) or through-fall, where water drips to the ground. Secondary interception occurs at ground level where water hits undergrowth. Some water returns to the atmosphere via evapotranspiration.
Water lost from vegetation via both evaporation and transpiration. Click on the boxes below to reveal definitions of both terms:
The amount of water that could be lost by evapotranspiration. For example, this is potentially high in deserts, but the amount that can take place is limited due to the minimal moisture available. Actual evapotranspiration is what actually occurs. In the UK there is more water available for evapotranspiration than takes place.
Where water slowly soaks into the soil from the ground. The maximum rate at which this can occur is known as infiltration capacity (mm/hour) and it is dependent on the amount of water already present in soil structure and vegetation.
The most important input into the system forms includes snow, hail, rain, and fog.
Water in the soil does not remain there but moves down slowly into the lower layers of soil and rock. It creates groundwater storage found in rocks and this may later be moved sideways through the rock via groundwater flow.
Water flows through the hydrological cycle in various ways:
Throughflow: where water moves downwards through layers of soil.
Channel flow: downhill movement of water in rivers.
Groundwater flow: Lateral movement of water from the water table.
Boulders collide with one another as they move down the river, and can break into smaller pieces. Over time rocks become more rounded in appearance.
Water moving slowly through the ground.
The lowest point to which erosion by running water can occur.
Can be either exogenetic or endogenetic, and moves by sliding, saltating, or rolling.
Glaciations and changes in rainfall.
When a river picks up material and then rubs it against its bed and banks. Erosion occurs by the process of abrasion. Most effective during times of flood. Main method of both vertical and horizontal erosion.
River sediment deposited as a river enters lake, lagoon or ocean.
Volume of water flowing in a river at a particular point, during a particular period of time.
Held in solution and can come from erosion, pollution, mineral springs and chemical weathering.
Area of land that is drained by a river.
Found by dividing total length of all streams in a basin (L) by its area (A).
Drowned lower part of a river, as it enters the sea.
Water lost from vegetation via both evaporation and transpiration.
Water held in the ground.
Force of water that hits river banks, and then pushes water into cracks. Air becomes compressed, pressure increased and the riverbank may, in time collapse.
This is when plants prevent some rainfall from directly reaching the ground, for example, water on leaves.
Where water slowly soaks into the soil from the ground.
Length of time between peak rainfall and peak discharge.
Water flowing overland, often as a result of land being saturated.
Water in the soil does not remain there but moves down slowly into the lower layers of soil and rock.
The amount of water that could be lost by evapotranspiration.
Changes in the flow of a river throughout that occur with different seasons.
Pebbles, sand and gravel are lifted up by the current and bounced along the bed.
A continual process, which is as a result of the chemical composition of the water.
Graphs that show how a drainage basin responds to a period of rainfall.
Suspended sediment load
Carried with the body of the current.
Very small particles of clay and silt are carried in suspension.
Where land is uplifted after plate movement or volcanic activity.
Larger boulders rolling or sliding along the riverbed. Only experienced in times of great flood.
Loss of water from plants.
Where water moves downwards through layers of soil.
Dividing line between drainage basins (usually higher ground).