Natural Stream Processes Guide No. 03 Streams in their natural state are dy- agency officials, and others to start a recycle nutrients from natural pollution namic ecosystems that perform many thoughtful inquiry into the true source sources, such as leaf fall, to purifying beneficial functions. Natural streams of local stream management problems. the water. The natural stream tends and their flood plains convey water The material contained in this guide to maintain itself through the flushing and sediment, temporarily store excess makes evident that the source of many flows of annual floods that clear the flood water, filter and entrap sediment stream problems is in the watershed, channel of accumulated sediments, and pollutants in overbank areas, far from the main stream channel. debris, and encroaching vegetation. recharge and discharge groundwater, Landowners, local officials, and oth- Extreme floods may severely disrupt naturally purify instream flows, and ers concerned with streams need to the stream on occasion, but the natural provide supportive habitat for diverse work together across property lines balance of the stream ecosystem is plant and animal species. The stream and jurisdictional boundaries to find restored rapidly when it is in a state of corridors wherein these beneficial func- suitable solutions to stream problems dynamic equilibrium. tions occur give definition to the land and to implement practices to protect, and offer “riverscapes” with aesthetic restore and maintain healthy stream qualities that are attractive to people. ecosystems. CHANNEL FORMING Human activities that impact stream AND RECONDITIONING ecosystems can and often do cause STREAMS ARE problems by impairing stream functions PROCESSES and beneficial uses of the resource. DYNAMIC ECOSYSTEMS Solving stream management problems Flowing water contributes sig- requires knowledge and understanding Streams in their natural condition nificantly to erosion and the shaping of of the stream’s natural processes, and typically exist in a state of dynamic most land masses. During the evolution since many problems originate beyond equilibrium. When a stream is in dy- of a landscape, stream characteristics the banks, a watershed approach. namic equilibrium, the amount of sedi- develop including: drainage density, This Ohio Stream Management ment delivered to the channel from the stream order, and longitudinal profile Guide provides an overview of the watershed is in long-term balance with (Figure 1). Erosion in watersheds un- stream’s natural processes and of the the capacity of the stream to transport affected by human disturbances takes human impacts on stream ecosystems. and discharge the sediment. A balance place at geologic rates. During any The information provided here can be also exists between communities of given year, the majority of waterborne used by land managers, watershed aquatic organisms inhabiting a stream sediment is redeposited within the groups, river conservationists, public and the biochemical processes that watershed as colluvium at the base WATERSHED BOUNDARY 1 1 1 1 3 2 BASIN 3 DIVIDE 3 2 1 4 1 1 2 1 1 3 1 ION OS 2 1 ER AGGREGATION BASIN 1 OUTLET 1 1,2,3,4 = STRAHLER’S ALLUVIUM STREAM ORDER MOUTH OF STREAM (a) PLAN(a) VIEW Plan OF viewBASIN of basin (b) LONGITUDINAL(b) Longitudinal PROFILE ALONG profile MAIN along STREAM main stream Figure 1. Drainage Basin and Longitudinal Profile Along Stream Bankfull flows play long-term regime of climate, landform, STORM RAINFALL a primary role in form- geology (including soils) and resultant TIME TO PEAK FLOW ing and reconditioning vegetation. Each channel reach has PEAK FLOW channels. Bankfull flows its own unique history of flow condi- in natural watersheds of tions and regime factors giving rise URBANIZED WATERSHED CONDITION humid areas, like Ohio, to its general features. A river system occur about every 1.5 may contain many different channel PEAK FLOW years on average. The full types each transitioning from one to NATURAL WATERSHED CONDITION range of rising and falling another. REDUCTION IN discharges associated Natural channels can be broadly BASE FLOW with these runoff events grouped into alluvial channels and is involved in the channel hard-bed or rock-bed channels. The STREAMFLOW DISCHARGE, Q forming and recondition- bed and banks of alluvial channels TIME, T ing processes. The fre- consist of riverine deposits that allow Natural watershed condition with high quency of bankfull flows for relatively rapid adjustment of chan- infiltration capacity, large amount of basin nel geometry in response to changes storage, and long travel time for runoff to may increase significantly reach stream station of hydrograph with changes in land use, in flow conditions and sediment load. disrupting stream stability. Hard-bed or rock-bed channels are Urbanized watershed condition with low infiltration capacity, minimal amount of basin Flood flows along streams relatively resistant to down cutting but storage, and short travel time for runoff to in response to precipi- may have alluvial banks that allow for reach stream station of hydrograph tation are a function of rapid lateral adjustments. Sediment many factors including: deposits may cover portions of a hard- Figure 2. Hydrographs of Streamflow Discharge basin area, infiltration ca- bed or rock-bed channel giving it the Before and After Urbanization pacity, and time of travel appearance of an alluvial channel. of slopes or as alluvium and sediment of flows (figure 2). Basins Alluvial channels in a given drainage bars along streams. The amount of with high infiltration capacity and a long basin tend to share similarity in their sediment discharged from the basin time of travel, tend to generate peak hydraulic geometry, that is, the mean generally represents a small percent- flood flows of lesser magnitude than depth, top width and velocity relation- age of the gross erosion occurring in those in similarly sized drainage areas ships for typical cross sections. Coarse the watershed. Longitudinal profiles of with lower infiltration capacities and materials characterize alluvial channel channel bottom elevation from stream shorter time of travel. beds in headwater areas; fine materials mouth to headwater divide typically dominate the lower channel reaches. exhibit upward concavity with steepest CHANNEL TYPES AND Natural channels in plan view can gradients in headwater areas and flat- be considered to be either straight, test gradients toward the mouth. This PATTERNS meandering or braided. The distinc- concave shape is the end result of tion between straight and meandering erosion and deposition as the stream General features of natural streams channels depends on the degree of matures. are the result of physical, chemical sinuosity, that is, the ratio of channel Down cutting or incising of a stream and biological processes reflecting a length to valley length. Channels with by erosion is ultimately controlled by its ���������������� ������� ������������������ base level, that is, the elevation of a �������������� ������� �������������� grade control such as resilient bedrock or the confluence with a larger, stable stream of the channel network. A stream ���� ��������� that has adjusted its longitudinal profile ���� to a local base level, sediment load and ��������� ��� �������� flow regime, and is no longer degrading ���� (down cutting) or aggrading (rising due to sediment deposition) is referred to as ���� ���� a poised or graded stream. Under these conditions, the amount of sediment de- livered to the stream is in balance with �������� ������ the capacity of the stream to discharge ���� it. During periods of medium and low �������� flow, tributaries may deliver sediment to the main channel where it is deposited as bars at the confluence until a flood occurs giving the main stream sufficient energy to dislodge and transport the Figure 3. Plan View of Staright, Braided and Meandering Channel Forms. sediment downstream. sinuosity greater BOUNDARY OF MEANDER BELT than 1.5 are gener- ally considered to be SINE WAVE BANK BANK OVERFLOW meandering. Braided PATTERN BUILDING EROSION CHANNEL channels contain sediment bars that cause multiple chan- nels to form during EROSION- low-flow conditions. RESISTANT DEPOSIT Straight, meandering EXISTING or braided channels CHANNEL FUTURE CHANNEL E POSITION may change from O AK XBOW L SILTED one form to another OXBOW over time such that a continuum exists between the three Figure 4. Meandering Stream in an Alluvial Floodplain channel patterns (Figure 3). the continuity equation, the energy equation, and Manning's equation. Meander forms of alluvial streams The continuity equation expresses tend to exhibit sine wave patterns of STREAM FLOW one of the fundamental principles of predictable geometry, but non-unifor- DYNAMICS stream flow dynamics. It states that mities in the alluvial deposits along the discharge passing a channel cross streams and flood plains generally Flow in natural channels normally section is equal to the cross-sectional disrupts the regular pattern. Nonuni- occurs as turbulent, gradually-varied area multiplied by the average veloc- formities consisting of erosion resistant flow. Under conditions of gradually- ity of flow. Average velocity is used materials can slow the progression varied flow, the stream’s velocity, cross- in the equation because velocity is of bank erosion at meander bends section, bed slope, and roughness vary not uniformily distributed in a chan- causing cutoffs and oxbow channels