Geochemical/hydrochemical evaluation of the geothermal potential of the Lamongan volcanic field (Eastern Java, Indonesia)
© Deon et al. 2015
Received: 19 May 2015
Accepted: 1 October 2015
Published: 26 October 2015
Magmatic settings involving active volcanism are potential locations for economic geothermal systems due to the occurrence of high temperature and steam pressures. Indonesia, located along active plate margins, hosts more than 100 volcanoes and, therefore, belongs to the regions with the greatest geothermal potential worldwide. However, tropical conditions and steep terrain reduce the spectrum of applicable exploration methods, in particular in remote areas. In a case study from the Lamongan volcanic field in East Java, we combine field-based data on the regional structural geology, elemental and isotopic composition of thermal waters, and the mineralogical and geochemical signatures of volcanic rocks in exploring hidden geothermal systems. Results suggest infiltration of groundwater at the volcanoes and faults. After infiltration, water is heated and reacts with rocks before rising to the surface. The existence of a potential heat source is petrologically and geophysically constrained to be an active shallow mafic-magma chamber, but its occurrence is not properly reflected in the composition of the collected warmed spring waters that are predominantly meteoric in origin. In conclusion, spring temperature and hydrochemistry alone may not always correctly reflect the deep geothermal potential of an area.
In a conventional approach, several methods need to be adopted and integrated to understand the geochemical and geophysical signatures of active geothermal systems (e.g., Rybach and Muffler 1981). These methods also apply for greenfield studies and include: (a) geochemical investigations, e.g., application of chemical geothermometers to infer the temperature of the geothermal reservoir; measurement of gas isotopes, such as 3He/4He, to constrain the origin (mantle or crust) of fluids; (b) drilling of exploration wells; (c) gravity measurements to map any negative anomaly associated with the steam fraction in high-porosity reservoir rocks or to locate zones of lowered density provoked by thermal expansion in magmatic bodies; (d) application of electrical methods such as resistivity to search for zones of higher-salinity fluids; (e) use of seismic methods for the localization of shallow intrusions and estimation of their vertical extension.
Gunung Lamongan (8.00°S, 113.342°E, and 1625 m above sea level) is one of several active volcanoes located in East Java. During the nineteenth century, Gunung Lamongan (last eruption in 1898) was among the most active volcanoes in Indonesia and seismic activity is ongoing since then (Carn 2000).
Java is located on the Sunda Arc that forms part of the Indonesian Archipelago between the landmasses of Eurasia and Australia at the NE margin of the Eurasian Plate. The Sunda Arc is a volcanic belt that has formed as result of the subduction of the Indo-Australian Plate beneath the Eurasian Plate, with a rate of ~6 cm a−1 (Hamilton 1979; Puspito and Shimazaki 1995). It extends from the Andaman Islands north of Sumatra to the Island of Alor in the Banda Sea, covering a distance of more than 3000 km (Carn and Pyle 2001). Subduction in the Sunda Arc started in the early Eocene (Katili 1975; Hamilton 1979; Rangin et al. 1990). Java hosts 90 Holocene volcanoes, with the Merapi in West Java as one of most active volcanoes worldwide. An E–W trending chain of more than 30 modern volcanoes forms the central spine of Java. The rocks building up the volcanoes classify as tholeiitic, calc-alkaline, and high-K calc-alkaline and alkaline suites (Whitford et al. 1979). Basalt and basaltic-andesite constitute the dominating rock types, mainly composed of anorthitic plagioclase, pyroxene, and minor olivine.
The early Cenozoic mountain arc: today uplifted and partially eroded. It is one of the few exposures of arc-related crystalline basement built up by Cretaceous ophiolites. Arc rocks are thick (>2500 m) and are spread over a distance of 50 km.
The Kendeng basin: this poorly exposed region is characterized by a strong negative Bouguer anomaly, which extends all the way to Bali. This anomaly becomes less negative around the modern volcanic arc. It is E–W oriented for at least 400 km parallel to the southern mountains. It is filled by volcanoclastic turbidites and pelagic mudstones.
The Sunda shelf: the area was explored for hydrocarbon exploration. Between 2000 and 6000 m of Eocene to Pliocene shallow marine clastic and extensive carbonate sedimentary rocks were deposited within fault-controlled basins.
Lamongan volcanic field (LVF) of East Java represents a volcanic region with numerous cindered cones and maars. The LVF is situated at the transition zone between the compression-dominated subduction zone to the south and the extension-dominated back-arc region Masalima to the north, forming the Java Sea. Two previous studies (Carn 2000; Carn and Pyle 2001) investigated the morphologic, petrologic and geochemical characteristics of the maars and cindered cones, but did not involve geothermal field studies. Maars and cindered cones formed when magmas came in contact with water, causing a phreatomagmatic eruption associated with pyroclastic fallouts and flow deposits (Heiken 1971; Fisher and Waters 1970; Moore et al. 1966). Some of the maars in the Lamongan area are NW–SE oriented, comparable with the strike of the Tiris fault (Carn 1999). The Lamongan volcano is located in a structurally complex area and was very active until approximately 14,000 years ago. The volcano is composed of three different vents: Tarub, Tjupu and Lamongan itself (Carn 1999). Tarub is the oldest cone and detached from the younger stratocone of Lamongan by a prominent NW–SE depression, which is most likely fault related. Recent studies have shown that Lamongan belongs to the reviving volcanoes in Indonesia, as seismic activities have recently increased (Chaussard and Amelung 2012).
Tiris is a small village located on the eastern flank of Mount Lamongan. Several warm springs occur in close proximity. They have temperatures ranging between 35 and 45 °C (Deon et al. 2012, 2013), which are ~10 °C warmer than the surrounding groundwater. Because of this temperature difference, we supposed that the area hides a geothermal potential hard to be exploited due to the difficult field conditions.
Rainwater may have been trapped in the pyroclastite layers and could have build horizons which previously interacted with the magma beneath the Lamongan and possibly represents one part of the fluids available in the area. One should consider the location of LVF approximately 20 km from the coast. In the area, several lineaments and faults are known (Carn 1999). Thus, it is beyond doubt that a considerable water infiltration may have occurred sometime in the past.
Topography, morphology, and hydrogeology
The area of Mt. Lamongan is characterized by a steep terrain landscape and dense tropical vegetation. Geological mapping of the area is challenging due to difficult access and the occurrence of severely weathered rocks at the surface. For instance, the outcropping basaltic rocks experienced intense lateritization. Heavy rain from December to May and a dry period from May to October characterize the climate in East Java. Moreover, significant variation of the precipitation rate exists depending on the elevation area. The annual precipitation in Pasuruan approximately 40 km NW of the study area at 15 m above sea level (a.s.l.) is 1300 mm/year. In Klakah, situated S of Mt. Lamongan at 250 m a.s.l., it is about twice that much, i.e., 2400 mm/year (Sporrer 1995). The steep area is sparsely populated and access to outcrops and hot springs is difficult. The fluid sampling locations refer to the following altitudes (a.s.l.): springs Tiris 1 to Tiris 6 = 510 m; spring WP7 = 382 m.
Field work and sampling
The fieldwork around the Lamongan area covered an area of about 16 km2 and included the systematic structural measurement of the strike direction of fractures. In particular, fractures were measured in the area around Lamongan after the last volcanic activity in March 2012. Lineaments could not be recognized in the field, but are evident in aerial photographs.
Magmatic rocks were sampled around Mt. Lamongan volcano; water samples were collected from the main river (Tancak), springs, maars, and from the sea (outside the investigation area; Figs. 1, 2). The springs Tiris 1–6 are located along the Tancak river. Water samples were collected from seven warm springs both east (Tiris 1–6) and north-east of the volcano (WP17), the Tancak river (WP18), and from the lake Ranu Lading (WP7 lad). Seawater was sampled on the coast north of the town Probolinggo (WP5). Figure 2 compiles the sampling sites around the volcano. The water samples were collected according to the procedure of Giggenbach and Goguel (1989) and Marini (2000) recommended for the quantitative analysis of the major ions and isotopes of oxygen, hydrogen, and strontium. Water samples were filtered using a 0.45 µm membrane filter to prevent the interaction of the fluid with suspended particles and algal growth. For the analysis of anions and isotopes, water samples were untreated, while for cation analysis, the water samples were acidified with HNO3. Water samples collected for major ions and Sr-isotope analyses were stored in small polyethene bottles, while for isotope analysis of H and O, the samples were stored in glass bottles.
Mean values of the field parameters of water samples
Altitude (m a.s.l.)
Electron microprobe analysis (EMPA)
Single-spot mineral analyses were performed using a CAMECA SX100 electron microprobe operating in the wavelength-dispersive mode at the Electron Microprobe Laboratory, Department of Inorganic and Isotope Geochemistry at the Helmholtz Centre Potsdam—German Research Centre for Geosciences (GFZ) in Potsdam, Germany. The analytical conditions include an accelerating voltage of 15 kV, a beam current of 10 nA, and a focused beam. Well-characterized grains of plagioclase, olivine and pyroxene were used as standards. Secondary-electron (SE) images were collected with a JEOL JXA 8230 electron microprobe (15 kV accelerating voltage) in the same laboratory.
X-Ray diffraction analysis (XRD)
To determine the modal mineralogy of the rocks by XRD, the rock samples were crushed and sieved to obtain the 63-µm fraction. XRD patterns were recorded in transmission using a fully automated STOE STADI P diffractometer (Cu-Kα radiation), equipped with a primary monochromator and a 7°-wide position sensitive detector, at the Department of Chemistry and Physics of Earth Materials at GFZ. The diffractograms were refined with the EXPGUI-GSAS software (Larson and Von Dreele 2000; Toby 2001; Belsky et al. 2002), using reference structures from the ICDS database (Bergerhoff and Brown 1987). Additional X-ray measurements (step-scan mode) were performed with an automatic Siemens D500 diffractometer (half automatic beam—40α, Graphite secondary monochromator—with Cu Kα 40 kV, 35 mA) at the Section of Material Research and Physics, University of Salzburg, Austria.
X-ray fluorescence analysis (XRF)
XRF analyses were conducted at the Department of Inorganic and Isotope Geochemistry at Helmholtz Centre Potsdam—German Research Centre for Geosciences, using a PANanalytical AXIOS instrument featuring a 4 kW Rh tube. Additional XRF data were acquired at the Section of Material Science and Physics, University of Salzburg, on a Bruker S4 Pioneer instrument, equipped with a 4 kW Rh tube. Major elements were determined at reduced tube energies. Counting times were chosen such that the relative 2σ uncertainties were less than 1 % for Si and Al, and less than 5 % for elements occurring at the 1–10 wt% concentration level. For the determination of trace elements, tube conditions and counting times were optimized automatically up to 4 kW and 400 s per element, to obtain a detection limit of ~3 ppm (3σ). Typical errors (2σ) from the counting statistics were 1–2 ppm at low concentrations (<10 ppm), ~5 ppm at the 100 ppm concentration level, and better than 50 ppm at the 1000 ppm level.
Stable-isotope (D–O) analysis
δ D and δ 18O measurements were performed at Alfred Wegner Institute, Helmholtz Centre for Polar and Marine Research, Potsdam, Germany. The water samples (3 mL) were analyzed using a Finnigan MAT Delta-S mass spectrometer equipped with two equilibration units for the simultaneous determination of hydrogen and oxygen-isotopic composition. In one sequence, 48 water samples (including standards) were measured in two equilibration units with 24 sample positions each. The first position of each unit was equipped with the measuring standard water. Three standards were used for quality control. Measuring and control standards were selected according to the expected isotopic composition of the samples. The isotope data were corrected linearly compared to the standards if necessary. The 1σ standard deviation ranges from 0.03 to 0.08 (O) and from 0.2 up to 0.8 (D).
Sr-isotope measurements of rocks (basalts and carbonates) and waters were performed at Geosciences Centre, University of Göttingen, Germany. For Sr-isotope analysis of volcanic rocks, about 100 mg of powdered samples was digested in a mixture of 40 % HF and 65 % HNO3 at 100 °C. After complete dissolution and evaporation, the sample residue was dissolved in 6 N HCl at 100 °C and again evaporated. The sample residue was then re-dissolved in 2.5 N HCl for further treatment using ion-exchange chromatography. For the analysis of thermal waters, about 2 mL of water was evaporated and re-dissolved in 2.5 N HCl. A sample of CaCO3 was directly dissolved in 2.5 N HCl. Separation of Sr from other cations was done on quartz-glass columns using Biorad AG 50 × 8 (200–400 mesh) resin and 2.5 N HCl. Purified Sr-fractions were loaded onto out-gassed Re filaments using 0.25 N H3PO4 and measured on a Finnigan MAT262 thermal ionization mass spectrometer (TIMS). 87Sr/86Sr ratios were corrected for instrumental fractionation using the natural 88Sr/86Sr ratio of 8.375209. Routine standard measurements yielded an average 87Sr/86Sr ratio of 0.71040 ± 0.00002 (2σ: n = 15) for the NBS987 standard. Only distilled reagents were used for chemical sample preparation. Blanks were less than 0.5 ng for Sr. The reproducibility of the individual 87Sr/86Sr ratio was equal to or less than 0.00003 (2σ).
Chemical composition (mg/L) and stable-isotope and 87Sr/86Sr-composition of ground and thermal waters sampled during the field campaigns
WP17 Oct 2012
Tiris 1 June 2012
Tiris 2 June 2012
Tiris 3 June 2012
Tiris December 2011
Tiris 5 June 2012
Tiris 6 December 2012
WP7 Lad June 2012
WP18 June 2012
WP 5 June 2012
Diluted and contaminated seawater
Silica-geothermometers applied to the water samples
Mineralogy and petrology of the volcanic rocks
Bulk rock composition (wt%) of basalts and carbonates and their initial Sr-isotopic signature
Modal composition (wt%) of basalts
The thermal water sampled in the area can be classified, according to the Giggenbach diagram, as bicarbonate water. It is the first sampling in the area of Mt. Lamongan. However, springs from the nearby Argopuro volcanic complex show a higher sulfate content, higher temperatures and a lower pH (Pertamina Geothermal Energy 2015, pers. Comm.). This would indicate an active magma chamber and a heat source located beneath the Argopuro volcano and defines the Lamongan area as an outflow region from the Argopuro volcanic complex.
Isotope ratios show a basically meteoric origin of the sampled groundwater. High element concentrations and increased salinity are caused by strong alteration processes, along with high dissolution rates in the center of the geothermal field at Argopuro. Groundwater is transported and cooled down towards the discharge area and arises in hot springs, which show lower temperatures and higher HCO3 concentrations. Relatively high Li and B concentrations are typical for basaltic-andesite rock formations (Nicholson 1993). Potassium shows concentrations typical for geothermal-alteration patterns, characterized by the formation of illite, smectite, or kaolinite (Brehme 2015). Low SO4 values are due to the location of springs in the outflow zone. Sulfate minerals generally precipitate in low-pH springs occurring in the center of the geothermal field (Fig. 11). Generally, the WP 17 spring has slightly different Na/Cl ratios than Tiris 1–6 springs. Tiris 1–6 springs are located closer to the geothermal center, which let them cluster at higher concentrations of, i.e., Cl, Na, and B. It is interesting to note that the Mg content is elevated in the water from the springs in the proximity of the river running through basalts (Tiris 1–6). Their higher temperature facilitates the solution of Mg from these rocks.
The chalcedony geothermometer suggests a reservoir temperature of ~130 °C, which is reliable considering that the springs are located in an outflow area of a magmatically influenced system. Comparable systems, as the Lahendong geothermal field, which is controlled by young volcanism, show slightly higher reservoir temperatures in the center of the field (Brehme et al. 2014). However, the Lahendong field also shows temperatures of 140 °C in the outflow area (Brehme et al. 2014, 2015).
Kim et al. (2003) describe a geothermal setting similar to Tiris for the Jeju volcanic island in South Korea. The occurring lithologies share the properties of the rocks of the Tiris geothermal area: high permeable pyroclastites underlying less permeable basaltic lava. In the LVF, the pyroclastic units must have been derived from previous eruptions of Mt. Argopuro and the overlain fractured basalts are the products of the subrecent effusive activity of Mount Lamongan (nineteenth century). Faults and fractured rock play a major role in development of geochemical characteristics of the geothermal field (Brehme et al. 2015 submitted). Presumably, groundwater is migrating through the permeable pyroclastites, following pathways to the surface through predominant faults or fracture patterns. On its way to the surface, the water becomes slightly heated and equilibrated with the mafic rocks, as implied by the virtual identity of their 87Sr/86Sr-isotopic composition. Interaction with a mantle-related source is further implied by the excess of HCO3 −, since carbonate rocks are unknown in the study area and the only origin of HCO3 − could be explained by the degassing of mantle-derived magmas. This preliminary field study should be succeeded by subsurface exploration to improve the knowledge of the LVF geothermal system.
The occurrence of highly permeable pyroclastites overlain by basalts supports the existence of a concealed layer, as described by Hochstein (1988), which could be responsible for capturing H2S, accounting for the HCO3 − excess of the springs located in the outflow zone of the system. According to Chaussard and Amelung (2012), the Lamongan field belongs to the volcanoes with the world’s highest uplift areas evidenced by InSAR data, indicating magmatic activity in the subsurface. Lamongan might host potential hydrothermal resources, however, these are not expressed by surface manifestations, such as hot springs with T > 50 °C, steam grounds, or fumaroles as in other regions in Indonesia. The frequent occurrence of maars and cinder cones is related to the interaction of magma and hot water; however, the maar-water temperature is the same as the groundwater temperature in the area (29 °C). In addition to passive seismic recording and more comprehensive fluid sampling, shallow drillings are mandatory to evaluate the geothermal potential in this area. Lamongan likely constitutes the outflow area of a larger system, with the nearby Argopuro being the upflow area of this system. In this area, springs with substantially higher temperatures and lower pH values occur, fingerprinting the existence of an active magma chamber at depth. Due to concession and legal issues according to Indonesian law, these data are not open for publishing and thus, could not be used here. It becomes, therefore, challenging to link and proof the conclusions of this survey campaign. Our exploration study demonstrates that greenfield exploration based on hydrochemistry may fail to correctly evaluate the deep geothermal potential in tropical areas rich in meteoric water, and has to be succeeded by other site-specific exploration work.
FD carried out the field work, measurements and the interpretation. FD is the principal investigator. H-J F contributed to the interpretation of the rock geochemistry and gave relevant contribution in the manuscript writing. MB contributed to the water geochemistry interpretation and geothermometer application. BW carried out the strontium isotopes measurements and wrote the methods part related to this measurement. TS performed the cation and anion analyses on the water samples and supported the fluid chemistry interpretation. IM participated to the fieldwork and contributed to the geological interpretation. MSJ participated to the fieldwork. DP organized and supported the fieldwork. She is the leader of the oil and mineral resources agency for the province of Eastern Java. All authors read and approved the final manuscript.
The German Federal Ministry for Education and Research (BMBF) is thanked for funding this German project under the Grant 03G0753A. The continuous support of K. Erbas (Potsdam) as project coordinator is highly appreciated. Our thanks go to I. Pieper for the ICP water analyses at the TU Berlin; H. Meyer (Potsdam) for stable-isotope measurements on the water samples, and R. Naumann (Potsdam) and F. Finger (Salzburg) for XRF measurements. O. Appelt and I. Schäpan (Potsdam) are acknowledged for their support with the electron microprobe and SEM, respectively. A. Förster (Potsdam) and P. Möller (Potsdam) provided many suggestions that helped improving the manuscript. The authors would like to thank the anonymous reviewers for their interesting and important suggestions and comments. A major acknowledgement goes to the Agency for Oil and Mineral resources in Surabaya East Java province (DINAS-ESDM).
The authors declare that they have no competing interests.
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