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The base level of a river or stream is the lowest point to which it can flow, often referred to as the 'mouth' of the river. For large rivers, sea level is usually the base level, but a large river or lake is likewise the base level for tributary streams. All rivers and streams erode toward sea level, which is also known as the "ultimate base level." If a river is dammed, a new base level (the level of the reservoir) replaces the ultimate base level. As a result, the stream’s base level is raised. Consequently, this reduces the stream’s velocity, leads to deposition, and a reduction of the gradient upstream from the reservoir. A rather rare exception can be seen in the Jordan Rivermarker, for which the base level is the Dead Seamarker, 417 m below modern sea level.

Base level is also significant for subsurface drainage. A low base level is a prerequisite for the formation of karst topography, a network of sinkholes and caverns that can develop as slightly acidic groundwater enlarges joints (by solution) in limestone rock. Often this network of underground drainage feeds back to surface drainage along the edges of larger rivers, which are the effective base level.

When the source of a stream is very high relative to its base level (high stream gradient), erosion proceeds rapidly due to the energy of the rapidly moving water and the topography becomes rugged, and it is considered a young stream (geologically speaking). When erosion has acted for a long geologic time, wearing down the high points and making a small difference between the source and the base level of a stream (low stream gradient), then the stream is called mature. Mature stream valleys have gentle slopes, rounded higher points and meandering courses.

A very hard layer of rock can form a temporary base level, until it is cut through. For example, Lockport dolomite has created a temporary base level for the Niagara Rivermarker. Eventually this will be cut through as Niagara Fallsmarker recedes, and Lake Eriemarker will be drained to near the lower base level of Lake Ontariomarker.

Movements of land can greatly affect base levels. As an illustration, the uplift of the Colorado Plateau, combined with the opening of the Gulf of Californiamarker to the sea, established sea level as the base level for the Colorado Rivermarker and led to the (geologically) rapid erosion that resulted in the Grand Canyonmarker.

The many meanders of the Kentucky River show that it was a mature stream with little relief. Uplift of the central Kentuckymarker area rejuvenated the stream, causing it to cut a deep canyon, but preserving the meanders that indicate the stream existed prior to the uplift.

Other geologic processes can affect base levels. In the Finger Lakesmarker of New Yorkmarker, Ice age glaciation greatly deepened the lake valleys and rejuvenated tributary streams. These streams have deep ravines and often waterfalls where hard rock layers slow erosion; they are said to be hanging valleys.

Sea level can also change (primarily due to the formation or melting of continental ice sheets), and raise or lower the final base level for coastal rivers. Along the east coast of North America, river valleys extend out onto the continental shelf, indicating a time when erosion was possible due to the lower base level of a lower sea level in the past. Today many of these same rivers end in bays, indicating that sea level has risen in recent geologic time. This is referred to as a drowned coastline.


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