FLORIDA GEOLOGICAL SURVEY


The area of greatest decline was in the vicinity of well 808-155-2
where the secondary artesian aquifer is absent. Large fluctuationF
of the water table in this area indicate good recharge to the
Floridan aquifer and good hydraulic connection between the
aquifers.
 Hydrographs of water levels in wells east of the Green Swamp
area (figs. 23, 27, and 28, wells 810-136-2, 815-134-2, 815-139-3, and
822-138-2) show that the water table fluctuated between 5 and 10
feet during the period 1959-62. The water table occurs at depths
ranging from about 2 feet to more than 70 feet below land surface.
The area has a potentially large capacity to store rainfall. Water
moves downward from the nonartesian aquifer to the Floridan
aquifer in the Lake Wales Ridge and moves upward in the valleys
of Davenport and Reedy creeks. The best hydraulic connection
between aquifers in the eastern part of the Green Swamp area
probably occurs beneath the Lake Wales Ridge. This is indicated
by almost identical fluctuations of water levels in wells 815-139-2,
-3 (fig. 27).
 Water levels in wells and sinkhole lakes, located in the
southeastern part of the Green Swamp area, fluctuated about 5
feet (fig. 29). During wet periods, the water level is near or above
land surface and water is stored in lakes and swamps. During dry
periods, water levels decline due to lack of recharge and to pumping.
Water levels in the nonartesian aquifer are generally higher than
the piezometric surface indicating recharge to the Floridan aquifer.

 HYDRAULICS OF THE NONARTESIAN AQUIFER

 Permeability of a 3-foot section of the nonartesian aquifer
was determined in a well (810-144-2) in southeastern Green
Swamp and in a well (815-134-2) 5 miles east of Green Swamp by
using the slug test method (Ferris, 1962). The field coefficients of
permeability for the wells were determined to be about 50 gallons
per day per square foot (gpd/ft2) and about 40 gpd/ft2,
respectively. The results of laboratory tests of disturbed sand
samples collected from a test hole in the bottom of Lake Parker
near Lakeland (Stewart, 1959) ranged from 20 to 180 gpd/ft2
(table 8). The permeability of the aquifer is probably lower in the
interior of the Green Swamp area than in the surrounding ridges
because of greater clay content.
 The specific yield of the nonartesian aquifer was determined
using a graphical analysis of rainfall and water-table fluctuations