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Berlin Environmental Atlas

02.12 Groundwater Levels of the Main Aquifer and Panke Valley Aquifer (Edition 2017)

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Exact knowledge of the current groundwater levels, and hence also of groundwater stocks, is imperative for the State of Berlin, since the water for the public water supply of Berlin (approx. 221 million cu.m. in 2016) is obtained from groundwater. This groundwater is pumped at nine waterworks, almost entirely within the territory of the city. Only the Stolpe Waterworks on the northern outskirts obtains water from Brandenburg, but also supplies Berlin with approx. 9 % of the city's total intake (Fig. 1).

Figure 1
Fig. 1: Location of the waterworks which supply Berlin with drinking water, as of May 2017

Moreover, groundwater reserves are tapped for individual use and for process water, as well as for major construction projects, groundwater rehabilitation measures and heating-related purposes. Numerous instances of soil and groundwater contamination are known in Berlin, and they can only be rehabilitated on the basis of exact knowledge of groundwater conditions.

For this reason, the State Geology Working Group produces a map of ground-water levels every month, for internal use. The map for May, the month with normally the highest groundwater level, is published in the Environmental Atlas.

Definitions Regarding Groundwater

Groundwater is underground water (DIN 4049, Part 3, 1994) which coherently fills out cavities in the lithosphere, and the movement of which is caused exclusively by gravity. In Berlin, as in the entire North German Plain, the cavities are the pores between the sediment particles in the loose sediments . Precipitation water which percolates (infiltrates) into the ground first fills these pores. Only that part of the percolating water which is not bound as adhesive water in the non-water-saturated soil, nor used up by evaporation, can percolate to the phreatic surface and form groundwater. Above the phreatic surface, capillary water is present within the unsaturated soil zone; it can rise to various heights, depending on the type of soil (Fig. 2).

Figure 2
Fig. 2: Phenomenology of Underground Water
(from Hölting 1996)

Aquifers consist of sands and gravels, and, as incoherent material, make the storage and movement of groundwater possible.
Aquitards consist of clay, silt, gyttja and glacial till and, as cohesive material, hinder water movement.
Aquicludes consist of clay which is virtually impermeable to water.

If the potentiometric surface lies within an aquifer it is known as free or unconfined groundwater, i.e., the phreatic and potentiometric surfaces coincide. In cases of confined groundwater however, an aquifer is covered by an aquitard so that the groundwater cannot rise as high as it might in response to its hydrostatic pressure. Under these conditions, the potentiometric surface is above the phreatic surface (Fig. 3).

If an aquitard, such as a layer of glacial till, is located above a large coherent aquifer (main aquifer), surface-proximate groundwater may develop in sandy segments above the aquitard and in islands within it, as a result of precipitation. This is unconnected with the main aquifer, and is often called stratum water. If an unsaturated zone is located below the glacial till, it is called floating groundwater (Fig. 3).

Figure 3
Fig. 3: Hydrogeological Terms

As a rule, groundwater flows at a slight incline into rivers and lakes (receiving bodies of water) and infiltrates into them (effluent conditions; Fig. 4a).

Figure 4a
Fig. 4a: Groundwater infiltrates into bodies of water (effluent conditions)

In times of flooding, the water surface is higher than the groundwater surface. During such periods, surface water infiltrates into the groundwater (influent condition). This is known as bank-filtered water (Fig. 4b).

Figure 4b
Fig. 4b: Bank-filtered water caused by flooding: Surface water infiltrates into the groundwater (influent conditions)

If in the neighbourhood of these surface waters, groundwater is discharged via wells, so that the phreatic surface drops below the level of that body of water, the body of water will also feed bank-filtered water into the groundwater (Fig. 4c). The amount of bank filtration is between 50 and 80 % of the total water obtained in Berlin, depending on the location of the wells.

Figure 4c
Fig. 4c: Bank-filtered water caused by discharge of groundwater: due to the drop in the groundwater caused by wells, surface water infiltrates into the groundwater

The groundwater velocity of flow in Berlin is approx. 10 to 500 m per year, depending on the groundwater incline and the permeability of the aquifer. However, near well facilities, these low-flow velocities can increase significantly.

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