Hydrogeological Characteristics of Karst Maros:

Case Study - Saleh Cave

Ivan Taslim

, A. M. Imran

, Sakka

Program studi Geografi, FST, Universitas Muhammadiyah Gorontalo

Jurusan Teknik Geologi, Fakultas Teknik, Universitas Hasanuddin

Program studi Geofisika, Fakultas MIPA, Universitas Hasanuddin

Keywords: Hydrogeology, morphology, karst, geoelectric.

Abstract: Maros karst area known have a morphology similar a tower form, valley (doline, uvala) along cave with

underground river. This research aims to analyse the hydrogeology behavior of Maros karst area so it will

reveal existence of water potential. Method used in this research is geology survey there is fracture system

measure for getting joint dominant direction related to cave system development and underground river, along

with morphology identification to know the function as catchment area, aquifer and infiltration zone.

Geoelectricity method used to presume limestone structure and cave system base on value of resistivity. The

result reveal that the morphological of the research location implied in karst hill with macro type (eksokarst)

positive form that is tower karst and negative form that is ponor, also many speleothem (endokarst). Analysis

of fissure system orientation found two (2) common direction at Saleh Cave that is northeast to southwest

direction it’s about 65

NE–245

SW where the joint direction relatively having the same direction with dry

channel and southeast to northwest direction it’s about 140

SE -320

NW where the underground cave system

have the same way. Geoelectricity interpretation indicate the cave system and underground river reside in

about 18-45 meter below surface. Hydrogeology behavior of Maros karst at Saleh Cave very dependent by

morphology condition, also development of fissure structure

1 INTRODUCTION

Karst is a landscape in carbonate rocks that are very

typical form of hills, valleys, doline, uvala, polje,

caves system and the existence of underground river

network. Karst morphology is formed by tectonic and

dissolving processes resulting in numerous fractures

in limestone that have a role as vertical inlet and the

development of underground rivers and concentrated

solubilization (Haryono, et al., 2004). The formation

of karst areas is influenced by climatic, tectonic and

lithological factors. These three factors also play a

role in establishing the Maros karst area. Based on the

regional geological map (Sukamto, et al., 1982), the

constituent rocks of the Maros karst area are the

Tonasa formation carbonate rocks that were Eocene -

Miocene (51 - 16 million years ago).

Maros karst area according to Daryanto, et al.

(2009) is influenced by the geological structure due

to the limberation (karstification) process of

limestones so as to form various kinds of outer

formation (eksokarst) such as upright hills, dolina

valleys, resurgence, ponor or sinkhole, and formation

in it (endokarst) that can be encountered such as

stalactites, stalagmites, flowstones and underground

river systems. Physically, the Maros karst area is dry

and barren, so that the people living in the area suffer

from water shortages, especially in the dry season

(Setiawan, et al., 2008).

Imran (2006) mentions that underground rivers

emerge as surface or springs streams which are

further utilized by surrounding communities as a

source of life both for household needs and for

irrigation. According to Rachman (2010), the

dynamics of water resources potential of Maros karst

area shows a significant decrease indicator. This is

thought to be due to changes in landscapes and karst

cover areas that may result in the decline of karst area

function as rain catchment and surface water

absorption. Changes in landscapes and land cover

conditions in the karst area also have an impact on

climate change affecting karst aquifer function (Hao,

et al., 2006).

Taslim, I., Imran, A. and Sakka, .

Hydrogeological Characteristics of Karst Maros: Case Study - Saleh Cave.

DOI: 10.5220/0010040602070211

In Proceedings of the 3rd International Conference of Computer, Environment, Agriculture, Social Science, Health Science, Engineering and Technology (ICEST 2018), pages 207-211

ISBN: 978-989-758-496-1

207

The karst landscape is an area with a potential

water resource that flows beneath the surface as an

underground river. With the identification and

mapping of potential water resources in the karst area

should be done as an effort in the preservation and

management, in order to support the sustainability of

the surrounding community life. Saleh cave in

Pattunuangasue District Simbang District is included

in Maros karst area which has underground river

flow. The study entitled "Hydrogeological

Characteristics of Karst Maros Area: a case study of

Saleh Cave", aims to identify karst morphology in

relation to subsurface water resources, estimation of

Gua Saleh's system using geoelectric method and to

analyze the influence of geological structure (fracture

pattern) on underground river system at Saleh cave.

2 METHODS

The research location of Saleh Cave is located in

Patunuangasue area, administratively located in

Simbang District Maros Regency South Sulawesi

Province, with geographic position 5° 2' 59,40" S and

119° 43' 17,16" E. Data collection in the form of

geological structure measurement (random fracture

pattern) in Saleh Cave, and measurement of the

Wenner-Schlumberger configuration geoelectric

method above the Saleh Cave (Figure 1), with a

stretch of 160 meters, the distance of each 10 meter

electrode so as to know the subsurface condition of

Saleh Cave.

Figure 1. Geoelectric measurement scheme

The identification of karst morphology was

analyzed based on its shape and function as rain

catchment areas, aquifers and water absorption areas

below the surface. Geoelectricity measurement data

is processed by using Res2Dinv software then

interpreted with reference to correlation between

resistivity value and rock. The solid measurement

data is processed by using Dips software so that the

general direction (fracture pattern) in Saleh Cave is

obtained.

3 RESULT

3.1 Geoelectric Methods Measurement

This method is based on the measurement of the

electrical properties of the rock, ie the type resistance

shown in the form of cross-section of 2D images. The

image cross section is obtained after the measurement

data is processed by using Res2Dinv software.

Interpretation of the 2D cross-sectional image refers

to the table of rock correlations and resistivity values

(Telford, et al., 1990), to determine the subsurface

condition of Saleh Cave. The result of the

measurement inversion in the form of 2D cross-

section shows the depth of geolistrik penetration

about 30 meters below the surface with variation of

resistance value of type around 2.0 Ωm to >4,718

Ωm.

Measurement of track 1 above Cave Saleh with

coordinates 119° 43' 15.83" E - 5° 2' 56.9" S and 119°

43' 17.37" E - 5° 3' 0.74" S is at a surface height of

about 150 - 167 above a sea level (asl) with

northwest-southeast direction. The result of

measurement on track 1 (Figure 2) can be interpreted

that there is a resistivity value of 2.0 Ωm to 132 Ωm

at a depth of 2 meters-25 meters (electrode 2-8) and a

depth of 20 meters-25 meters (between electrode 11 -

14) is a layer of limestone that has a geological

structure (stocky) that allows surface water to

infiltrate (infiltration) through a fissure or crack

system. This layer has good porosity with permeable

properties that can serve as storage media and water

infiltration (epicarstic aquifer). Resitivity values

>132 Ωm to 1071 Ωm at depths of 2 meters-30 meters

(electrode 6-15) indicate the presence of layers with

geologic structures that are thought to be massive

limestones with poor impermeable porosity. Higher

resistivity values of >3,053 Ωm at depths of 2 meters

to 20 meters (between 8-14 electrodes) and depths of

25 meters to 30 meters (electrode 10-13) are thought

to be layers of limestone that have widened cavities

as a result of a prolonged dissolution process to

collapse and form a cave passage. The detected cave

passage is estimated to be a new section of the roof at

a depth of 30 meters (between 10-11 electrodes).

Measurement of track 2 above the Saleh Cave

with coordinates 119° 43' 15.25" E - 5° 2' 57.05" S

ICEST 2018 - 3rd International Conference of Computer, Environment, Agriculture, Social Science, Health Science, Engineering and

Technology

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and 119° 43' 16.32" E - 5° 3' 0.79" S is at a surface

level of about 150 asl-165 asl in the direction

Northwest-southeast. The result of measurement on

track 2 (Figure 3) can be interpreted that the

accumulation of water in the limestone layer near the

surface to a depth of 20 meters (between 2-8

electrodes) with a resistivity value of 4.06 Ωm to 89.4

Ωm. The limestone layer has good porosity with

permeable properties allowing water to flow through

the fissure or crack system and also become a water

storage medium (epicarstic aquifer). Resitivity values

>89.4 Ωm to 700 Ωm at depths of 2 meters-28 meters

(electrode 5-14) show the presence of layers with

geologic structures that are thought to be massive

limestones with poor impermeable porosity. Higher

resistivity values of about >1,958 Ωm at depths of 10

meters to 30 meters (between 7-13 electrodes) are

thought to be layers of limestone that have

wavelengths that have been dilated as a result of long-

lasting dissolution processes until collapse, and

formed a cave alley. The detected cave aisle is

estimated to be a new section of the roof that is at a

depth of 18 meters to 30 meters (between 9-13

electrodes).

Measurement of track 3 above the Saleh Cave

with coordinates 119° 43'15.67"E - 5° 3'0.21"S and

119° 43'19.23 "E - 5° 2'58.05"S is at a surface level

of about 140 asl - 162 asl with the West-West-East-

Northeast direction. The result of measurement in

track 3 (Figure 4) can be interpreted that there is

accumulation of water in the limestone layer which

has a geological structure (stack) from the surface to

a depth of 25 meters, which is indicated by a

resistivity value of 12.1 Ωm to 294 Ωm (between 5-

14 electrodes). The limestone layer has porosity both

with permeable properties, can serve as storage

medium and epicarstic aquifer media through fissure

or crack system. Resitivity values >294 Ωm to 1,447

Ωm on surface to a depth of 15 meters (between 2-7

electrodes) and a depth of 5 meters to 20 meters

(between electrodes 6-12) indicate a layer with a

geologic structure that is thought to be a massive

limestone with bad porosity impermeable. Based on

the results of the plot of the Saleh Cave and the 3 geo-

electric track scheme, a resistivity value of about

3,211 Ωm at a depth of 10 meters (between 8-9

electrodes) is a proper Cave Saleh entry slot above the

measuring site. Medium resitivity value >3211 Ωm at

depth of 25 meter to 30 meter (electrode 10-13)

allegedly is a layer of limestone forming cave

passageway associated with Saleh Cave entry.

Measurement of track 4 above Cave Saleh with

coordinates 119° 43'16" E - 5° 3'0.62" S and 119°

43'20.30" E - 5° 2'59.61" S is at a surface level of

about 150 asl - 168 asl with the Southwest-East

Northeast. The result of measurement on track 4

(Figure 5) can be interpreted that there is a resistivity

value of 11.8 Ωm to 362 Ωm at depths of 10 meters

to 15 meters (electrode 4-5) and a depth of 2 meters

to 15 meters (between electrode 6 -14) is a layer of

limestone that has a geological structure (stocky) that

allows surface water to infiltrate (infiltration) through

a fissure or crack system. This layer has good porosity

with permeable properties that can serve as storage

media and water infiltration (epicarstic aquifer). The

resitivity value >362 Ωm to 2005 Ωm on the surface

to a depth of 25 meters (between 2-13 electrodes)

shows the presence of layers with geologic structures

that are thought to be massive limestones with poor

impermeable porosity. Medium higher resistivity

value of >4718 Ωm at a depth of about 30 meters

(between 5-7 electrodes) is thought to be a layer of

limestone that has a cavity that has undergone

widening as a result of a long dissolution process to

collapse and form cave hallway.

Figure 2. Track result 1

Figure 3. Track result 2

Figure 4. Track result 3

Water

accumulatio

Cave

Massif

Limesto

Epicarstic Zone

icarstic Zone

Massif

Limestone

Water

accumulation

Roof of Cave

Massif

Limestone

Water accumulation

icarstic Zone

Roof of Cave Entry

Hydrogeological Characteristics of Karst Maros: Case Study - Saleh Cave

209

Figure 5. Track result 4

3.2 Fracture Patterns Measurement

The result of the solid measurement was obtained by

the dominant direction of Northeast-Southwest about

NE-245

SW where the solid direction is relatively

unidirectional with dry cave passages and North-

West-trending alleys about 140

SE -320

NW where

the solid direction is relatively unidirectional with

underground river flow aisle (Figure 6). In addition to

the solubility of rocks, thickness and degree of

cohesiveness of rocks, the direction/pattern of general

fracture is also one of the controlling factors for the

formation of alleys and the availability of

underground rivers at Saleh Cave. This fracture

pattern system can be caused by tectonic influences

which are then widened by the dissolution process

due to climatic influences (rainfall). The relationship

between the fracture pattern and the formation of cave

and underground passageways is usually

characterized by the dissolution of the upper part of

the rock where the limestone surface is in an

unsaturated state of CO

thus causing the flow of

water to be dominated by vertical flow through rock

crevices.

Figure 6. Fracture Patterns (Rosette plot)

4 CONCLUSION

Based on the results and discussions that have been

described previously and refers to the objectives and

problems of research, it can be concluded that the

geomorphology at the study site included in the hills

tower karst Maros. The phenomenon of karst

morphology include (eksokarst): Tower karst,

Sinkhole and Ponor/resurgence; and (endokarst):

Stalactite, Stalagmite, Heliktit, Drypery, Flowstone,

also the presence of underground river flow. The

formation of karst morphology has an important role

in the process of surface water drainage, storage and

replenishment (storage and recharge) to infiltration

through the fissure field to the subsurface which is

ultimately channeled through the conduit as flow

underground river. The geological structures have

two general directions, the first relative to the

northeast-southwest of about 65

NE-245

SW where

the coarse direction is relatively unidirectional with

the dry cave passage and the general direction of the

second - necked Southeast-northwest direction

around 140

SE-320

NW where the relative in the

direction of the underground river basin.

Interpretation of measurements of geoelectric method

is known that the limestone layers below the surface

of Saleh Cave have varying resistivity values ie low

to high. Where a low resistivity value is interpreted as

a limestone layer that has a geological (muscular)

structure with porosity both permeable and high

resistivity values are interpreted as a massive

limestone coating with poor porosity is permeable.

It is suggested that there is further or continuous

(comprehensive) research on hydrogeology in the

Karst Maros Area in Pattunuangasue and in the

surrounding karst areas, to reveal the availability of

underground rivers as a potential groundwater. For

the identification of underground systems and

underground river networks in the karst area by

geoelectric method should be measured (data

retrieval) in sunny weather conditions and taking into

account the distance of the path and electrode to

obtain a more accurate subsurface description and can

then be compiled with the results of the cave

mapping.

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