Abstract
The cave passages formed in Donomulyo sub–district are formed in epigenic and hypogenic conditions in coastal areas. The dominant factors form the morphological condition of the cave passage that is the existence of structural factors, underground water flow, and tectonism that affect the condition of the passage. Structural factors form the existence of linement that affect the cave passage. Underground water flow forms a passage due to the change of vadose, epipreatic, and phreatic conditions. The existence of tectonism leads to the removal of limestone into several levels of cave passage development, in addition, there is the collapse of blocks, plates, talus, and sheets. The development of the cave passage level is also related to surface physiographic, which is connected to 5 levels with marine terrace, including 244–325 masl (level 1), 182–244 masl (level 2), 111–181 masl (level 3), 30–110 masl (level 4), and 0–29 masl (level 5). The development of fifth level shows that the level limit is located in the Sengik Cave, the fourth level is located in the Jebrot Cave, and the second level is located in the Banyu Cave, these three caves are the output of the underground rivers.
Highlights
The physiology of the southern java mountains stretches from Yogyakarta to the western part of Blambangan in the eastern tip of East Java
Donomulyo sub-district is located in the southern java mountains (Figure 1), which was composed of Wonosari formation in the form of coral limestone, silty limestone, tuffling limestone, sandy limestone, marl, peaty black clay and calcirudite
The cave passage formed a morphology in the form of elliptical passages and gorges that were accompanied by rubble, this was seen from cross section calculations which showed that the cave passage formed due to structural and hydraulic processes occurring in various cave passages
Summary
As a result of the lifting process, the limestone sediment that interspersed with volcanic rocks in the sea rose into the mountains. Donomulyo sub-district is located in the southern java mountains (Figure 1), which was composed of Wonosari formation in the form of coral limestone, silty limestone, tuffling limestone, sandy limestone, marl, peaty black clay and calcirudite. The Wonosari formation overlaps the Campurdarat formation and other old rock units. The thickness of this rock unit is around 80 m and 200 m [2]. Lifting and folding may occur again in PlioPliotosen, followed by a process of denudation. This tectonic activity only resulted in tilting the Wonosari Formation to the south with 10o inclination angle [3]
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