RECENT THEORIES OF CAVERN DEVELOPMENT
In recent years there has been an important
transition from the physiographic theorizing and qualitative reasoning of the
”classic” theories to a more quantitative process approach. Many recent studies
have investigated the geologic setting, the hydrology, and the chemical and
mechanical weathering and erosional processes associated with cavern and karst
development. The reader is referred to the comprehensive works by Jennings
(1985), Sweeting (1973), Ford and Cullingford (1976), White (1988) and Ford and
Williams (1989).
According to Ford (1981), it is now recognized that there is not one
general case of limestone cavern development that can be precisely defined as
older theories would have it. Rather, there are three common cases, the
predominantly vadose cave, the deep phreatic cave and the water table cave
(Figure 1).
The type or types of common cave development that occurs is governed by the
frequency of fissures significantly penetrated by groundwater, and by the joint
to bedding plane ratio. Together these characteristics combine to form the
concept of hydraulic conductivity. Hydraulic conductivity is a coefficient of
proportionality describing the rate at which water can move through a permeable
medium (Fetter, 1980). The higher the hydraulic conductivity, the more likely a
water table cave will develop. Water table caves are particularly common in
flat-lying rocks, where the perching of groundwater occurs because of the
presence of more resistant rock layers. Deep penetration of water is inhibited
by the presence of shallow open bedding planes which are continuous to springs.
Vadose type caves develop where sufficient streams collect above sink points
and transport water to the water table or a spring. Deep phreatic caves attain
their optimum development in steeply dipping rocks because continuous bedding
planes guide water to greater depths.
Palmer (1984) noted that larger passages of many caves show a succession of
levels with the youngest, and still active ones, lying at the lowest elevation.
The level in which enlargement occurs is concentrated at or near the
contemporary river levels. Studies in Kentucky by Miotke and Palmer (1972),
have shown that cave patterns are a reflection of numerous changes in base
level and climate since the Late Tertiary Period (Figure 2).
Palmer (1984) also noted that cave development is possible above, at, or below
the water table. Where caves form is dependent upon local geology, and
hydrology, and it is possible for one cave to have passages formed above, at or
below the water table. He further point out that a clear relationship in many
areas between cave levels and fluvial history, shows the tendency for much of
the solutioning to take place at the water table.
The evidence cited here from various karst researchers makes it clear
than an evolution of ideas has occurred pertaining to cavern speleogenesis. The
debate among early investigators as to whether caves originate at, below, or
above the water table has essentially been resolved. It is now accepted that
all three origins are possible depending on local hydrologic and geologic
conditions.