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Reservoir Review of the Rendingan-Ulubelu-Waypanas (RUW) Geothermal Field, Lampung, Indonesia

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Reservoir Review of the Rendingan-Ulubelu-Waypanas (RUW) Geothermal Field, Lampung, Indonesia GRC Transactions, Vol. 37, 2013 Reservoir Review of the Rendingan-Ulubelu-Waypanas (RUW) Geothermal Field, Lampung, Indonesia Suharno Geophysical Engineering Department, the Faculty of Engineering, Lampung University, Bandar Lampung, Indonesia Keywords and a southern (Ulubelu) section. With extension of the survey Rendingan-Ulubelu-waypanas, hydrothemal-mineral, fluid- area to include the Waypanas manifestations, this combined study inclusions, two phases, cooling area is now called the Rendingan-Ulubelu-Waypanas (RUW) geothermal system. My study of this area used geological, geophysical and pa- ABSTRACT leohydrological methods to obtain a four dimensional picture of the reservoir. Geological assessment consisted of surface studies, The Rendingan-Ulubelu-waypanas (RUW) geothermal sys- including field surveys of hydrothermal manifestations and rock tem contains host rocks that alter very readily because of the sampling; cores and cuttings were examined in hand specimen and great contrast between their hydrothermal environment and the petrographically, boreholes drilled, down hole temperatures and volcanic conditions under which they formed. Most surface rocks pressures measured and interpreted. Geophysical work consisted are weathered but some have also been altered hydrothermally. of micro-earthquake, gravity and magnetic data that have been The alteration includes both replacement of primary phases and analyzed to interpret the RUW reservoir. The microearthquake the products of processes that affected ascending thermal fluids. analysis contributed information that helped characterize the Alkali chloride water of near neutral pH once deposited silica hydrothermal system. The gravity data helped reveal the distribu- sinter at the surface but now acid steam condensate is forming tion and dimensions of host rocks within the geothermal system kaolin, silica residue and other phases. The mineralogy, fluid and nearby, and the magnetic studies the extent of the geothermal inclusions and surface manifestation indicate that conditions in system with respect to its rock alteration intensity. The RUW the RUW geothermal system changed spatially and temporally during its lifetime. The mineralogical evidence incompletely re- cords some of the changes in the thermal regime. The identities of the hydrothermal minerals reflect the new environment in which reservoir rocks find themselves. The main hydrothermal mineral assemblages were produced by neutral pH waters. The Th values are higher than the present well temperatures suggesting cooling has occurred since the inclusions formed. The RUW reservoir contains vapor, two phase and liquid dominated domains but is overall a liquid-vapor dominated system. This is revealed by the well measurements (T and P) and the hydrothermal alteration and fluid inclusions geothermometry. I. Introduction The Rendingan-Ulubelu-Waypanas (RUW) geothermal system is near circular in shape, as revealed by its magnetic signature, and extends over a distance of 15 km at the southern end of the Su- Figure 1. Surface geology and stratigraphy of the Tanggamus Regency. matra Fault Zone in Tanggamus, Lampung. Formerly this system Semangka Fault is a part of the end SE of Sumatera Fault System. Key to was known as Ulubelu. However, Pertamina (1992) suggested it stratigraphy is given in Table 1. Dashed and full lines are inferred and should be separated into two parts; a northern section(Rendingan) confirmed faults; modified from (Amin et al., 1993; Suharno, 2003). 471 Suharno Figure 2. The reservoir boundary model of the Rendingan-Ulubelu-Waypanas (RUW) geothermal system approximated from Suharno (2000, 2003). Solid ellipse is the Ulubelu caldera. Dashed line ellipses are geothermal prospects (RI, Rendingan; RII, Ulubelu; RIII, Waypanas). Qa: Alluvium, AtR: Altered rocks, TgAl: Tanggamus andesite lavas, KrRl: Kurupan rhyolite lavas, Dt: Da- cite tuff, RdAl: Rendingan andesite lavas, RdPr: Rendingan pyroclastics, TgLb: Tanggamus laharic breccia, KbPr: Kabawok pyroclastics, DdDl: Duduk Da- cite lavas, KkBAl: Kukusan basaltic andesite lavas, SlAl: Sulah andesite lavas, QTr: Ranau Formation, Tmgr: Granodiorite, Tomh: Hulusimpang Formation. Filled circles (Kk1): bore holes; stars: hot springs or fumaroles; triangles: sum- mits of mountains; squares: petrographic samples. Boxes are villages. Solid and dashed lines are confirmed and inferred faults, respectively. reservoir contains vapor, two phase and liquid dominated domains but is overall a liquid dominated system. This is revealed by the well measurements (T and P) and the hydrothermal alteration and fluid inclusion geothermometry. II. Materials and Methods a. Geology of Tanggamus Region The Tanggamus Region is located in Lampung Province, in southern Sumatra, Indonesia Its western edge occurs at the southern end of the Sumatra Fault Zone, which is marked by the Semangka River (Figure 1). This system trends along the main axis of the western part of the island. The Semangka Fault extends to the Sunda Strait, along the Semangka River into Semangka Bay and southwards. The geology of the Tanggamus Region is illustrated in Fig- within the Tanggamus Regency. Tanggamus volcanic rocks de- ure 1. The stratigraphy (Table 1) is divided into rocks of three rived from a ring of volcanoes comprising Mts. Tanggamus (1.5 broad age ranges: i.e. pre-Tertiary, Tertiary and Quaternary (Amin Ma), Kabawok (1.7 Ma), Waypanas (3.9 Ma), Kukusan (3.9), et al., 1994). The pre-Tertiary successions are the oldest exposed Sulah (4.5 Ma), Rendingan (1.4 Ma) and Kurupan (1.4.Ma); Mt. rocks, and are of regional extent. They include a low to medium Duduk (3.9) is in its center (Figure 1) (Suharno, 2003; Hidayatika grade metamorphic sequence of the Gunungkasih Complex (Amin dan Suharno, 2011). et al., 1994). The oldest rocks (Paleozoic) in this succession The highest part of the RUW study area is in the southeast, are nowhere exposed, however, and have almost certainly been with the summit of Mt. Tanggamus at approximately 2000 m asl, displaced by post-metamorphic faulting. This occurred in the late Table 1. Summary Stratigraphy of the Tanggamus Region. From Suharno (2003). Paleozoic or early Mesozoic. The No Unit (symbol) The Ages Lithology Thickness Menanga Formation is in contact Unconsolidated material, boulders, sand, 1 Alluvium (Qa) Holocene ? with the metamorphic basement silt and clay (Amin et al., 1994). The Quater- 2 Ranau Formation (QTr) Holocene to Pleistocene Pumeceous tuff 100-500 m nary succession comprises late 3 Recent volcanic (Qhv) Holocene to Pleistocene Andesitic basaltic lava, tuff and breccia, ± 800 m Pleistocene to Holocene lavas, 4 Older volcanic (Qv) Pleistocene Volcanic breccia and lava flow ± 400 m breccias and tuffs, reef limestone 5 Semong Formation (QTse) Pleistocene to Pliocene Sandstone-claystone (20-40 m) and Holocene alluvium sedi- 6 Kasal Formation (QTk Pleistocene to Pliocene Poorly consolidated volcaniclastics ± 200 m Pliocene to late- 7 Simpangaur Formation (Tmps) Badded sandstone and claystone (200-700 m) ments. Geological studies have Miocene been made by van Bemmelen 8 Bal Formation (Tmba) Miocene Tuffaceous volcaniclastics (100-200 m) (1949), Katili (1985) and Masd- 9 Granodiorite (Tmgr) Miocene Granitic pluton ? juk (1997). Mocene to late Interbedded sedimen: clay-stone, silt- 10 Seblat Formation (Toms) ± 500 m Oligocene stone & sandstone b. The Tanggamus Mocene to late Interbedded sedimens: clay-stone, 11 Gading Formation (Tomg) 100-500 m Volcanic Area Oligocene siltstone & sandstoene Hulusimpang Formation Mocene to late Volcanism occurs in the 12 Volcanic breccia and lava ? (Tomh) Oligocene northeastern part of the Se- Pandean pluton & related 13 Late Cretaceous Graitic pluton ? mangka Fault. The Semangka intrusives (Kgr) Fault is the SE part of the end 14 Menanga Formation (Km) Early Cretaceous Shale, cllaystone & sandston ? of Sumatra Fault System. The Gunungkasihn 15 Palaeozoic Undifferented metamorphic rocks ? volcanic system partly occurs Complex (Pzg) 472 Suharno and nearby the summit of Mt. Kabawok, at close to 1600 m asl. 100oC. The Waypanas manifestations between 700 and 400 m asl The summit of Mt. Rendingan at the 1700 m asl, is located in the south of Mt. Kukusan to the southwest of the Mt. Waypanas have northern part of the area. The lowest locations are around 100 to the same types of manifestations (Figure 2). 300 m asl, southwest of Mt. Waypanas. Most of the central part Thermal fluids ascend through the host andesites beneath of the study area is about 700 to 800 m asl within the volcanic ter- the sinters within moderately steep terrain in the central part of rains of Mts. Tanggamus, Kabawok, Waypanas, Kukusan, Sulah, the study area, close to Pagaralam village (Ulubelu manifesta- Rendingan and Kurupan (Figure 2). tions). But some out-flows discharge 7 to 15 km to the south and southwest of the study area (Waypanas manifestations) at lower c. Surface Expression of the RUW Geothermal System elevations (Figure 2). Insight into the RUW reservoir can be recognised from its surface expression. The geothermal system is situated within areas III. Result of high relief, around 1600-400 m asl, but moderately steep terrain occurs in its central part, mostly from 700 m to 800 m asl. The a. Extent of the Reservoir lowest places are south and southwest of (the RUW) geothermal The RUW geothermal system (Figure 2) is a large system, manifestations, at about 400 m asl (Figure 2). covering an area of about 150 km2. Evidence for its extent includes surface manifestations
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