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Induced Seismicity of the Groningen Gas Field: History and Recent Developments K

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Induced Seismicity of the Groningen Gas Field: History and Recent Developments K Induced seismicity of the Groningen gas field: History and recent developments K. van Thienen-Visser1 and J. N. Breunese1 Abstract For the large Groningen field, the first seismic event was Induced seismicity of the Groningen gas field is caused by recorded in 1991. The largest magnitude was an ML 3.6 event the production of gas. Because of the large areal extent of the on 16 August 2012. Even though the magnitude of the event reservoir, the long history of depletion, and the available data sets was, seismologically speaking, not high, intensities as high as VI (which exist as a result of consequences and public unrest caused were observed because of the shallow depth of the event (3 km, by induced seismicity), the field presents a valuable case for i.e., reservoir depth) and the soft surface soils in the area (TNO, studying the relationships among geologic, flow-dynamic, geo- 2013a), causing damage to houses in the area. mechanical, and seismological models. Gas production from the Until 2012, a maximum magnitude of 3.9, with a probabil- Groningen field started in 1963. Induced seismicity of the field ity of exceedance of 16% (van Eck et al., 2006), was seen as the first was recorded in 1991 (ML 2.4). During the subsequent 10 upper size limit for induced seismicity in the north of the Nether- years, induced seismicity stayed at a rate of about five events (ML lands. However, since 2003, seismicity in the field has increased ≥ 1.5) per year. Starting in 2003, the number of events and mag- in number and magnitude. It has become increasingly clear that nitudes started to increase. In 2012, the largest event (ML 3.6) induced seismicity of the Groningen field is nonstationary and occurred, which caused the most damage to date. As a conse- increases with time (Muntendam-Bos and de Waal, 2013). quence, studies carried out in 2013 have fundamentally changed Because of the nonstationarity of the induced seismicity, the way to look at the relationship between induced seismicity and maximum magnitude cannot be defined from statistical data gas depletion. There appears to be a close link between induced analysis only. Therefore, the need arose for fundamentally dif- seismicity and reservoir compaction resulting from extraction of ferent models that take the subsurface explicitly into account. gas. Because compaction manifests itself as surface subsidence, This has led to some studies in 2013 (for example, NAM, 2013; accuracy of the subsidence measurements is deemed much more TNO, 2013b) in which the links among the geology of the field, important than previously thought. The same holds true for qual- reservoir dynamics, and geomechanics have been investigated. ity and specific details of the static and dynamic models of the These studies have revised the assessment of induced seis- reservoir and its surroundings. In January 2014, it was decided to micity of the Netherlands, especially the Groningen field. The limit gas production in the central and highest-subsidence part of empirical relation proposed by Bourne et al. (2014) directly links Groningen field and allow more production from the less com- the cumulative compaction, which is highest in the center of the pacted field periphery. Seismicity observed in 2014 was markedly field, to seismicity. In TNO (2013b), compaction was shown to different from that in earlier years. Although not yet statistically react partly instantaneously on pressure changes, which provides significant, this observation suggests a close link among produc- a possible handle on the induced seismicity. tion, compaction, and seismicity. In January 2014, it was decided to reduce overall production of the Groningen field to 42.5 bcm in 2014 and 2015 and 40 Introduction bcm in 2016. More important, the production for five clusters of The Groningen gas field, in the northeastern part of the wells in the center of the field, corresponding to high compac- Netherlands, is the largest gas field in Western Europe, with gas tion values, was limited to 3 bcm per year for 2014 through 2017, initially in place (GIIP) of close to 3000 billion m3 (bcm). The field an 80% reduction from 2013 rates. was discovered in 1959 with the drilling of the Slochteren-1 well. We present an overview of the Groningen gas reservoir and From the start of production in 1963 through January 2015, 2115 its induced seismicity, using the relations among geologic mod- bcm (75% of the GIIP) had been produced. The field is still a major eling, reservoir-dynamic models, and geomechanical models. supplier of natural gas to the northwestern European gas market. The observations of 2014 are presented to assess the relation Since 1986, seismic events have been recorded in the north- between production and seismicity. ern part of the Netherlands, which is thought to be a tectoni- cally inactive region. The existing national seismic network was Geology expanded in the north of the Netherlands in 1992, with the first The Groningen gas field is on the Groningen High in north- borehole seismometer (five geophones at depths of 0 m, 75 m, eastern Netherlands, between the Ems Graben to the east and 150 m, 225 m, and 300 m). A further extension to 19 permanent the Lauwerszee Trough to the west. The structure formed during seismometers, which include 11 borehole seismometers in the the late Kimmerian extensional phase. Reservoir depth is 2600 to Downloaded 06/03/15 to 130.118.44.150. Redistribution subject SEG license or copyright; see Terms of Use at http://library.seg.org/ north, was implemented in 1995. Since 1986, seismicity in the 3200 m. The seal is formed by Zechstein salt covering the whole north of the Netherlands, ranging in magnitude from ML –0.8 of the field and varying in thickness from a few tens of meters to to ML 3.6, has occurred over various small gas fields and is con- more than 1 km. The reservoir consists mostly of Permian sand- sidered to have been induced by gas production. stones of the Upper Rotliegend Group. From south to north over 1TNO — Geological Survey of the Netherlands. http://dx.doi.org/10.1190/tle34060664.1. 664 THE LEADING EDGE June 2015 Special Section: Injection-induced seismicity the field, sediments change from mainly sandstone to more clay- being investigated (for example, Mossop, 2012; TNO, 2013b), stone. The thickness of the Rotliegend varies from ~ 100 m in the with reservoir compaction being a likely candidate. south-southeast to ~ 300 m in the north-northwest of the field. Three types of compaction models — time decay (Mossop, From east to west, thickness is relatively uniform (Mijnlieff and 2012), isotach, and rate-type compaction (RTiCM) in isotach Geluk, 2011; van Ojik et al., 2011; TNO, 2013b). formulation (TNO, 2013b) — have been fitted to the measured During the Kimmerian extensional phase, northwest-south- subsidence (TNO, 2013b). Figure 3 shows the fit to the measured east-oriented faults formed in the region (Figure 1). East-west-ori- subsidence for an optical-leveling point in the center of the field. ented faults formed before the Saalien unconformity. More than The estimates resulting from the compaction models for total 1800 faults (NAM, 2013) have been identified by using “ant track- subsidence differ by 5 to 10 cm. These compaction models all ing” of the 3D seismic cube. Only the 707 largest faults have been capture the delay at the start of production. The isotach model modeled. Density of the faults and orientations vary across the field. derived from shallow geotechnical models (Den Haan, 1994) fits The largest fault density is in the center of the field, predominantly the observed subsidence data quite well. The time-decay model oriented northwest-southeast. This area corresponds to the largest has been used previously in other gas fields in the Netherlands reservoir compaction and the area of the most induced seismicity. Subsidence Regulations require estimates of the amount of subsidence for each gas field in the Netherlands before production starts, with regular updates as production continues. The mining law of the Netherlands has a long history, having been implemented by Napoleon Bonaparte in 1810. The most recent revisions in mining law occurred in 2003. In the Groningen field area, sur- face subsidence is an important issue because the field is close to or below sea level. Groundwater levels and salinity, which are affected by subsidence, are important for the agricultural industry in the area. Furthermore, height and stability of nearby dykes are important to reduce the risk of flooding. The Groningen surface subsidence has shallow and deep causes. Shallow subsidence is caused by the compaction of clay, oxidation of shallow peat, and artificially modified groundwater levels. Deep subsidence results from reservoir compaction related to gas produc- tion. Because of gas depletion, the reduction of gas pressures causes compaction in the reservoir (Figure 2). The elastic properties of the overburden transfer the compaction almost instantaneously to the surface, and this is measurable as subsidence. The Groningen field covers a wide area (about 900 km2), and the subsidence bowl related to the production is quite extensive (about 40 × 50 km). Subsidence caused by compac- tion of the Groningen field has been measured since 1964 by using optical leveling. After the first campaign, which was lim- ited to the central and southern parts of the field, the bench- mark network was extended to the entire field, and density Figure 1. Top of Rotliegend (top of reservoir) with contour of the was increased for the second campaign of 1972. In 1987, the Groningen gas field in red. Black lines indicate modeled faults. White density of the optical-leveling network was improved further. lines show faults identified by using the ant-tracker algorithm of Petrel Until 2008, repeat surveys were performed every few years.
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