A review of oil and gas seepage in the Nuussuaq Basin, West Greenland – implications for petroleum exploration

Abstract

The Nuussuaq Basin in West Greenland has an obvious exploration potential. Most of the critical elements are well documented, including structures that could form traps, reservoir rocks, seals and oil and gas seepage that documents petroleum generation. And yet, we still lack a full understanding of the petroleum systems, especially the distribution of mature source rocks in the subsurface and the vertical and lateral migration of petroleum into traps. A recently proposed anticlinal structural model could be very interesting for exploration if evidence of source rocks and migration pathways can be found. In this paper, we review all existing, mostly unpublished, data on gas observations from Nuussuaq. Furthermore, we present new oil and gas seepage data from the vicinity of the anticline. Occurrence of gas within a few kilometres on both sides of the mapped anticline has a strong thermogenic fingerprint, suggesting an origin from oil-prone source rocks with a relatively low thermal maturity. Petroleum was extracted from an oil-stained hyaloclastite sample collected in the Aaffarsuaq valley in 2019, close to the anticline. Biomarker analyses revealed the oil to be a variety of the previously characterised “Niaqornaarsuk type,” reported to be formed from Campanian-age source rocks. Our new analysis places the “Niaqornaarsuk type” 10 km from previously documented occurrences and further supports the existence of Campanian age deposits developed in source rock facies in the region.

1 Introduction

The exploration potential for petroleum in the Nuussuaq Basin in West Greenland (Figs 1 and 2) was first realised in the early 1990s, based on the observations of oil seepage followed by core drilling and conventional exploration drilling (Christiansen 1993, 2011; Christiansen et al. 1994a, 1994b, 1995b, 1996a, 1996b, 1997a). However, we currently lack a full understanding of the petroleum systems of the area. Although oil seeps have been widely recognised on many coastal localities and classified in detail analytically (Bojesen-Koefoed et al. 1999, 2007; Christiansen et al. 1996c), we still do not know the areal distribution of mature petroleum source rocks in the subsurface and the vertical and lateral migration of oil and gas into possible traps or to the surface.

Fig. 1 Simplified geological map of the Nuussuaq Basin, West Greenland, showing the position of the outcropping sediments on Disko, Nuussuaq and Svartenhuk Halvø. EBF : Eastern Boundary Fault. Location of Umiivik-1 core is indicated. For the purpose of this paper, Nuussuaq Basin refers to the area shown in this figure.

Fig. 2 Simplified geological map of northern Disko and western Nuussuaq in the Nuussuaq Basin. Location of wells and cores with oil and gas, major and minor oils seeps, localities with various types of gas observations and the approximate position of the anticline from Sørensen et al . (2017; red-dashed line ) are marked.

Most recently, Sørensen et al. (2017) proposed a new play concept based on the photogrammetric mapping of inversion structures. A newly mapped large structural anticline on central Nuussuaq (Fig. 2) with expected good reservoirs and seals is an obvious exploration target if mature source rocks and migration pathways can be demonstrated. To understand this target and to provide the necessary input for a risk assessment, we need to further document oil and gas seepage in the inland areas, especially along and east of the Kuugannguaq–Qunnilik Fault zone in central Nuussuaq (Fig. 2). Compared to the numerous oil seeps along the coasts of Disko and Nuussuaq, only a few records have been obtained inland, where exploration logistics are more complicated and costs are higher. Also, freshly eroded rocks along the coast seem to better preserve oil than inland exposures, where volcanic rocks weather differently due to frequent melting and freezing processes and often alter to rocks with a distinct smell of soil.

Less attention has been paid to document the occurrences of gas in the Nuussuaq Basin, although some preliminary data were obtained during systematic analyses of boreholes drilled by the Geological Survey of Greenland (GGU), which later merged with the Geological Survey of Denmark to form the Geological Survey of Denmark and Greenland (GEUS) and industry. Unfortunately, in a number of these records, gas was not sampled and documented properly or at all. This paper presents a systematic review of all gas observations and data in the Nuussuaq Basin in order to understand the petroleum systems and aid future exploration. Here, we (1) summarise existing data for gas accumulations, much of which were, until now, only available in unpublished GGU and GEUS reports and (2) present new critical data based on samples collected in 2019. These new data are important to characterise oil and gas seepage near to the Kuugannguaq–Qunnillik Fault zone, where future drilling is being considered.

2 Geological setting and exploration models of the Nuussuaq Basin

The Nuussuaq Basin is a rift basin that developed during Cretaceous – Paleocene due to extension between Canada and Greenland. The basin is characterised by outcropping sediments on Disko, Nuussuaq and Svartenhuk Halvø. The southern limit is located around Qeqertarsuaq, Disko (Fig. 1), but the northern and western limits are less well defined. For the purposes of this paper, Nuussuaq Basin corresponds to the area shown in Fig. 1. The sediments of the Nuussuaq Basin and the overlying volcanic rocks are well exposed throughout the Disko–Nuussuaq–Svartenhuk Halvø region and are important to understand the sedimentology, stratigraphy, depositional and subsidence history of the sedimentary basins in West Greenland. The Nuussuaq Basin has been intensively studied as an analogue for offshore basins. Most of these studies are based on large field campaigns in 1991–1997 and 2004, combined with many shorter field trips (Christiansen 1993; Christiansen & Pulvertaft 1994; Christiansen et al. 1992, 1995a, 1996a, 1997a, 1998). For an overview of previous research and exploration history, see Dam et al. (2009) and Christiansen (2011).

The present paper focuses on the parts of the Nuussuaq Basin on western and central Nuussuaq between the Itilli and the Kuugannguaq–Qunnilik Fault zones (Fig. 2). In this part of the Nuussuaq Basin, the sedimentary succession is covered by a few kilometres of volcanics of the Vaigat and Maligât Formations (Figs 1–3; Pedersen et al. 2017, 2018). The underlying sediments were mainly characterised by drilling or from field work on exposures in the Itilli Valley, along the Itilli Fault zone (Figs 1 and 2).

Fig. 3 Simplified sedimentary and volcanic stratigraphy of the Nuussuaq Basin on Disko, Nuussuaq and Svartenhuk Halvø. The relationship between petroleum seeps and stains and main petroleum systems elements is shown. Possible ages for source rocks of the following oil types are shown: M : Marraat type; N : Niaqornaarsuk type; I : Itilli type; K : Kuugannguaq type. The Eqalulik type source rock is not known, but it is assumed to be early Cretaceous. Many of the petroleum stains in the Vaigat Formation are associated with later Eocene dykes. Vaigat Formation includes the following: An : Anaanaa Member; Na : Naujánguit Member; Or : Ordlingassoq Member. Note that the Eocene volcanic units are rather thin and not regionally distributed. Hareøen Formation is only found on Hareøen, Erqua Formation only on Ubekendt Ejland and Naqerloq Formation only on Hareøen and westernmost parts of Nuussuaq, Ubekendt Ejland and Svartenhuk Halvø. Based on Sørensen et al . (2017), Dam et al . (2009) and Pedersen et al . (2017, 2018).

The known sedimentary succession is dominated by marine sediments of mid-Cretaceous to Palaeogene age. A general facies change occurs from deltaic and slope sediments close to the Kuugannguaq–Qunnilik Fault zone to deeper marine turbidites in and around the Itilli Fault zone (Dam et al. 2009). Many mudstone intervals occur in the Itilli and Kangilia Formations (Dam et al. 2009); some of these may represent possible source rocks and many are likely to have good sealing capacities (Fig. 3). The most likely reservoir intervals are turbidite sandstones in the Itilli Formation and incised valley sandstones of the Quikavsak and Agatdal Formations and their equivalents (Dam & Sønderholm 1994, 1998; Dam et al. 2009; Hjuler et al. 2017; Kierkegaard 1998). The most likely traps are extensional-rotated fault blocks formed in the Cretaceous or Palaeogene, or late Paleocene inversion structures such as the anticline mapped by Sørensen et al. (2017).

Nuussuaq experienced a short, but very intensive, exploration phase in 1994–1998, driven largely by new, and at that time unpublished, data on oil seepage. The small Canadian company grønArctic Energy Inc. managed to drill four fully cored stratigraphic boreholes (GANW#1, GANE#1, GANK#1, and GANT#1) and one deep wildcat well (GRO#3) in 1994–1996. But, despite many encouraging oil shows and documentation of good reservoirs and seals in the Upper Cretaceous and Palaeogene succession, the company was unable to raise funding for further drilling and they eventually relinquished their licences in May 1998.

3 Existing data from oil seeps and bore holes in the Nuussuaq Basin

The first oil-seeps on Nuussuaq were discovered in the Marraat area in 1992 (Christiansen 1993). Since then, significant time and resources have been invested to find additional localities, especially along the coast, with evidence of either visible oil seepage or micro-seepage in mineralised veins. Oil seepage is very common in an area on western Nuussuaq (Christiansen et al. 1996c). Following the years of systematic field work, evidence of oil has also been found in many other localities, including Disko, Hareøen, Ubekendt Ejland and Svartenhuk Halvø (Figs 1 and 2).

Several hundred samples of oil seeps or oil-impregnated cores on Nuussuaq were analysed in detail by Bojesen-Koefoed et al. (1997a, 1999), and supplemented more recently by Bojesen-Koefoed et al. (2007). They described the characteristics of the oil samples from the region and grouped them into five distinct oil types. These types are adopted here, but for a complete overview of the oil-type classification, we refer the reader to Bojesen-Koefoed et al. (1999, 2007). The main models of source rock distribution, depositional environment and generative history of the source rocks are based on state-of-the-art analyses and are documented in detail (Bojesen-Koefoed et al. 1999, 2004, 2007; Christiansen et al. 1996c). Some of the oils have a unique composition of biological markers, containing organic compounds such as lupanes and a series of norhopanes that were only rarely documented at the time of analyses (Nytoft et al. 2000, 2002).

Understanding the distribution and concentration of different oil types is important for petroleum exploration on Nuussuaq. Previous studies demonstrated working petroleum systems and first indications of where the source rocks could be expected in the subsurface, where and when they have generated oil and how migration, and in some cases degradation, took place. The oils so far recorded in the Nuussuaq Basin occur in two main settings:

1. In oil-impregnated porous lavas and hyaloclastites that may have formed exhumed continuous reservoirs in the deeper part of the volcanic succession, especially within the Anaanaa Member of the Vaigat Formation (Pedersen et al. 1998) or just below, in the uppermost part of the sedimentary successions (Fig. 3). Oil-impregnated rocks hold large volumes of hydrocarbons, which were generated, and probably migrated vertically, from an underlying source rock such as oil of the “Marraat deltaic type" or the lesser known “Eqalulik type" or “Niaqornaarsuk type" (as defined by Bojesen-Koefoed et al. 1999). This migration likely occurred during and shortly after the main phase of volcanism in the region (62–60 Ma) with rapid subsidence and possibly increased heat flow. Such oils occur over large parts of western Nuussuaq, especially in the area from Marraat-1–GANE#1–Sikillinge (Fig. 2), where several billion barrels of more or less degraded oil may fill out most available porosity in the volcanics (Christiansen et al. 2006; see Supplementary File S6).
2. In migration conduits, especially along faults, dykes, fractures or as fluid inclusions in thin mineralised veins in many different volcanic units (Fig. 3). Oils also occur in some sands in the Asuk area on Disko (Fig. 2). Such oils are generally low in volume and concentration, but are known from large areas on Disko, Nuussuaq, Ubekendt Ejland and Svartenhuk Halvø, where they often belong to the “Itilli type," presumed to be generated from a marine mid-Cretaceous source rock (Fig. 3; Bojesen-Koefoed et al. 1999, 2007).

The first setting offers some possibilities for local exploration, especially in incised valley deposits of the Lower Paleocene Quikavsak and Agatdal formations on western Nuussuaq. The area of exploration interest is, however, rather small with complex structural features that are not likely to define large targets. The second setting suggests good exploration opportunities over much larger areas in the deeper part of the Cretaceous succession and supports the anticlinal model suggested by Sørensen et al. (2017).

The main area of known oil seeps and stains was significantly enlarged after numerous field seasons. It is likely that the area containing oil of the “Marraat type" can be further extended inland towards the north and northeast. The easternmost record of the “Marraat type" is the GANK#1 borehole. It is unclear whether this oil type can be traced further into the Kuugannguaq–Qunnillik Fault zone (Fig. 2). The main challenge for future oil seep studies is to find more examples from the second setting, especially along a possible fairway from northern Nuussuaq along the anticline to central and southern Nuussuaq. The major fault zones in the region are also interesting targets for future studies, as they may have been important migration pathways.

4 Existing records of gas in the Nuussuaq Basin

Well-documented analytical records of gas observations in the Nuussuaq Basin are relatively few. There are some historical observations of gas leakages from lakes or pingos, but they have not been analysed with modern analytical methods. More recent records were obtained during drilling campaigns, which revealed a high likelihood of widely distributed gas under pressure in the subsurface of the Nuussuaq Basin, either below a permafrost seal or deeper in the sedimentary succession. Since 1992, improved sampling techniques were developed for drilling and field work by the GGU and later by GEUS, which ensured a better understanding of gas distribution in the subsurface. Here, we review all known records of gas observations in chronological order and describe the various sampling techniques used, their limitations, to provide key results and make preliminary interpretations.

4.1 Numerous GGU boreholes, drilled in 1992

Numerous cores were drilled at Agatdalen (Fig. 2), Annertuneq (Fig. 2) and Svartenhuk Halvø (same location as Umiivik-1; Fig. 1) in 1992. These shallow fully cored boreholes were drilled to depths between 45 and 95 m by GGU using a custom-made light-weight rig that could be mobilised using small helicopters. The main goal was to document the presence of oil-prone source rocks within the marine Cretaceous succession (Fig. 3; Christiansen 1993; Christiansen et al. 1994c).

Core samples for gas analysis were taken in metal tubes. Results were reported by Laier (1994) in an unpublished institutional report, which is provided here as Supplementary File S1. Gas amounts were relatively low, which precluded stable isotopic analysis. Methane concentrations were low relative to ethane, propane and butane, which suggest preferential leakage of lighter molecules. For this reason, cans were used in subsequent studies, replacing the tubes. During the drilling at Annertuneq (core number 400407), white to bluish gas hydrates were observed at a depth of c. 7 m (Fig. 4). At the time of drilling, it was not realised that the material was gas hydrates and samples evaporated before they could be properly described and secured for analysis.

Fig. 4 Bluish gas hydrates at c . 7 m depth in core 400407 at Annertuneq on the north coast of Nuussuaq (location in Fig. 2). Core diameter is 3.0 cm. Photo taken on 1 August 1992.

4.2 Marraat-1 core, drilled in 1993

Marraat-1 (408001) core (location Fig. 2; sample numbers 408011 and 408020 in Table 1) was drilled by the Canadian company Falconbridge Ltd. for GGU in August 1993. It terminated at a depth of 448 m. The well was subsequently logged in October–November 1993 and some additional fluid samples of formation water were taken. The main goal was to clarify if the solid bitumen found at the surface was an indication of undegraded oil in the subsurface (Christiansen et al. 1994a; Dam & Christiansen 1994).

Table 1 Gas compositions for seven cores in the Nuussuaq Basin, West Greenland

Core (core number)	Sample number or core piece	Depth (m)	CH4 (ppm)	C2H6 (ppm)	C3H8 (ppm)	iC4H10 (ppm)	nC4H10 (ppm)	iC5H12 (ppm)	nC5H12 (ppm)	δ13C1 (‰)	δ13C2 (‰)	δ13C3 (‰)	δDC1 (‰)	Wetness	Gas origin	Data sources
Marraat-1 (408001)	4080111	41.0	28.9	0.08						−53.4				361	Th	Laier 1994; supplementary file S1 (also include additional analyses)
	4080201	82.0	37.1	0.10						−53.4				371	Th
Serfat (FP94-11-04)	3800022	290.0	1042	361	136	3.1	8.8	0.5	0.5	−11.2	−20.3	−20.9		2.1	Th HM	Laier unpublished data October and December 1994
	380003	290.2	2252	516	131	3.1	10.2	1.0	1.8					3.5		Supplementary files S2 and S3
	380004	290.4	2765	493	135	3.4	10.4	0.8	1.4					4.4
	380005	290.6	2306	541	168	4.7	14.0	1.0	1.5					3.6
	3800062	290.8	2006	481	155	4.8	13.0	0.9	1.5	−22.2	−23.7	−21.9		3.1	Th HM
GANW#1 (380101)	3801053	721.0	832 000	61 000	13 000	1500	1000			−43.3	−28.1	−27.1	−199.0	112	Th LM	Christiansen et al. 1995b
GANE#1 (439001)	4390073	631.0	823 000	28	8					−45.4				22 000	Th LM	Christiansen et al. 1996b (also include additional analyses)
	439001-368	633.7	44 400	333	330	67.3	144	28	18	−45.1				67	Th LM
	439001-530	689.8	9100	4						−40.9				2260	Th MM
GANK#1 (439201)	439201-054	194.5	46 700	2110	384	54	30.8	10.4	3.5	−49.5				18.7	Th LM	Christiansen et al. 1996b (also include additional analyses)
	439201-113	365.9	230 000	5300	1920	122	152	11	7	−46.9	−32.3			31.9	Th LM
	439201-118	379.7	133 000	4630	1540	140	122	24	8	−41.9				21.6	Th LM
GANT#1 (439101)	4391073	247.2	7600							−65.4				0	Biogenic	Christiansen et al. 1996b
	4391113	608.8	26 900	240	30					−34.8				100	Th HM
	4391123	608.8	642 000	410						−35.0				1566	Th HM
	439116	608.8	37 200	36	16.3	1.2	3.9	0.5	1	−37.0				711	Th HM
	439101-420	649.4	188 900	3350	562	68	192	30	18	−46.0	−30.4			48.2	Th LM
	439101-447	737.0	82 000	256	40.2					−40.1				277	Th MM
	439101-449	743.7	264 000	390	1600	86	242	28	39	−40.4				133	Th MM
	439101-4572	769.3	23 000	1560	278	8.8	21.7	1.9	2.6	−36.8				12.5	Th HM
	439101-458	774.0	107 000	1910	349	3	7	n.a.	n.a.	−39.7				47.1	Th MM
	439101-465	794.0	43 200	632	101	4.1	10.9	0.9	1.3	−39.1				58.9	Th MM
	439101-4722	816.2	38 800	193	82	5.7	10.3	0.9	1.3	−20.8				141	Th HM
	4391283	901.3	33 900							−68.0				0	Biogenic
Umiivik-1 (439301)		104.7	331 000	728	797	223	151			−51.2				217	Th LM	Christiansen et al. 1997b (all analyses)
		151.3	44 900	2650	782	215	84	34.7		−21.1				13.1	Th LM
		199.7	201 400	2020	464	tr	tr			−43.7				81.1	Th LM
		250.7	39 480	1750	599	39.5	56.7			−20.6				16.8	Th LM	Dam et al. 1998 (additional interpretation)
		307.7	148 000	2017	660	tr	tr			−38.9				55.3	Th LM
		403.6	77 500	2570	580	40	92			−24.6				24.6	Th HM
		450.5	68 500	3700	500	78	82			−21.9				16.3	Th PM
		752.5	404 200	17 600	1940	155	175			−31.8				20.7	Th PM
		794.0	43 920	6400	1280	167	124			−27.6				5.7	Th PM
		910.4	410 960	51 080	6540	590	293	29.6		−32.6	−27.9	−24.4		7.1	Th PM
		1065.6	49 940	5540	925	100	100			−20.1				7.7	Th PM
		1151.4	425 000	77 120	12 930	2470	1490	658	184	−35.1	−27.6	−23.6		4.7	Th PM
		1163.6	348 000	79 500	17 460	4000	2160	872	219	−34.6	−27.8	−24.6		3.6	Th PM
		1171.9	410 000	46 800	9340	2000	1400	622	200	−32.9	−27.6	−23.5		7.3	Th PM
		1182.6	38 960	9210	2910	690	570	250	92	−11.4	−20.7	−21.5		3.2	Th PM
		1197.9	313 000	2100	1270	270	258	95	41.5	−37.8	−22.2	−24.2		92.8	Th PM
1Contained high nitrogen. 2Differential leakage of C1 and light isotopes. 3Steel cylinder. tr: trace amounts. Blank cells indicate that the compound is not present (below detection limit) or that isotopes were not analysed. CH4 (C1): methane; C2H6 (C2): ethane; C3H8 (C3): propane; iC4H10: isobutane; nC4H10: n-butane; iC5H12: isopentane; nC5H12: n-pentane; wetness: C1/(C2 + C3); Th: thermogenic; LM: low-thermal maturity with respect to oil generation; MM: medium-thermal maturity with respect to oil generation; PM: postmature with respect to oil generation; n.a.: not analysed.

The subsequent analytical programme focused on the oil composition that suggested new models for age and depositional environment of the source rock (Bojesen-Koefoed et al. 1999; Christiansen et al. 1994b, 1996c). Some core pieces were sealed in cans for subsequent gas and formation fluid analyses. These data were reported by Laier (1994; see Supplementary File S1) and Christiansen et al. (1995b) and are summarised in Table 1. Two samples of a rather dry gas had a sufficient concentration of methane to allow analysis of stable carbon isotopes. Values of δ¹³C (¹³C/¹²C) and wetness indicate a mixed thermogenic biogenic origin (Table 1; Fig. 5).

Fig. 5 Wetness ( C 1 /C 2 +C 3 ) versus δ 13 C of methane ( δ 13 C 1 ) for Marraat-1, GANW#1, Umiivik-1 and Pingo 132. C 1 : methane; C 2 : ethane; C 3 : propane. Compositional fields indicate biogenic or thermogenic origin. Modified from Schoell (1984).

4.3 Falconbridge mineral exploration cores, drilled in 1994

During their mineral exploration programme for nickel sulphides in 1994, Falconbridge Ltd. observed gas bubbles and froth on core surfaces. They penetrated a zone of pressured gas at c. 290 m depth in one of the boreholes in the Serfat area (core number FP94-11-04; Fig. 2). The gas was found in Cretaceous sediments below thick sills on the north coast of Nuussuaq (Dam & Nøhr-Hansen 1995).

Five samples of gas were obtained from the cores and stored in plastic containers. Data were provided by Laier in October and December 1994 as unpublished data (see Supplementary Files S2 and S3, respectively) and are summarised in Table 1. The samples contained significant volumes of gas with relatively high concentrations (up to 3000 ppm) of wet gases. C-isotope composition of methane (δ¹³C₁), ethane (δ¹³C₂) and propane (δ¹³C₃) suggested a thermogenic origin from a source rock with a relatively high thermal maturity. The data suggested a loss of lighter isotopes by diffusion from the plastic containers (Table 1). This was tested by experiments of the containers (Laier, unpublished data, December 1994; Supplementary File S3).

4.4 GANW#1, drilled in 1994

GANW#1 (core 380101, Fig. 2) was drilled by grønArctic Energy, Calgary, Canada in September–October 1994 as a follow-up to the Marraat-1 borehole (Christiansen et al. 1995a). The main goal was to penetrate the base of the volcanic succession and to document further oil impregnation at depth.

One gas sample (380105) from a depth of 721 m was sampled from the wellhead in a steel cylinder, and a full suite of gas analyses was carried out. The data were reported by Christiansen et al. (1995b) and are presented in Table 1. The gas had a moderate wetness (Table 1; Fig. 5). δ¹³C₁ versus δD of methane (δDC₁) suggests a thermogenic origin from a source rock and an association with oil (Fig. 6), while δ¹³C₁ versus δ¹³C₂ suggests a low thermal maturity dominated by type III kerogen (Fig. 7; Christiansen et al. 1995b).

Fig. 6 δ 13 C of methane ( δ 13 C 1 ) versus δD of methane ( δDC 1 ) for GANW#1 and Pingo 132. Plotted compositional fields (blue lines) are from Jenden and Kaplan (1989).

Fig. 7 δ 13 C of methane ( δ 13 C 1 ) versus δ 13 C of ethane ( δ 13 C 2 ) for GANW#1, Umiivik-1 and Pingo 132. Maturity lines are calculated from Faber (1987) for type II kerogen. R o : vitrinite reflectance.

4.5 GANE#1, GANK#1 and GANT#1, drilled in 1995

Three fully cored boreholes GANE#1 (core 439001), GANK#1 (core 439201) and GANT#1 (core 439101) and one sidetrack (GANE#1A; data not shown here) were drilled by grønArctic Energy in the summer of 1995 to depths of between 398 and 901 m as part of their exploration and production license on western Nuussuaq (locations in Fig. 2). The main goal was to characterise the sedimentary succession below the volcanic succession and to demonstrate an active petroleum system. All boreholes revealed oil and gas within volcanic or sedimentary rocks. Detailed sedimentological and stratigraphical studies and comprehensive geochemical analyses of organic compounds were carried out by GGU for grønArctic Energy (Christiansen et al. 1996b). Some of these data are presented in Table 1.

Some gases sampled in steel cylinders together with gas from core-pieces sealed in cans were analysed. Gas was commonly observed in many intervals in GANT#1 and GANE#1, indicated by bubbles in the drilling fluids. Most notable was the gas flaring of GANE#1 at a depth of c. 660 m (see fig. 4 in Christiansen et al. 1996a). Corresponding cores from this drilling depth show oil impregnation with the relatively rare “Eqalulik type" that cannot be correlated to any known source rock (Bojesen-Koefoed et al. 1997a, 1999).

In GANE#1 (and GANE#1A), gas was commonly observed in several sandstone intervals (631–641, 684–689 and 696–702 m). In GANT#1, gas was commonly observed in many sandstone intervals between 575 and 775 m. Most of these gases are thermogenic in origin. But their variable composition suggests the presence of both low maturity gases from the penetrated succession and high maturity gases that may have migrated from deeper in the subsurface (Table 1).

4.6 Umiivik-1, drilled in 1995

Umiivik-1 (core 439301) was drilled as a 1200 m deep stratigraphic well by grønArctic Energy for GGU in August to September 1995. The main goal was to test and document a Cenomanian–Turonian source rock (Bate & Christiansen 1996; Dam et al. 1998). In the deeper part of the well, gas was heard to be escaping the core. Some intervals revealed a white froth on the core surface when it was removed from the core barrel (Bate & Christiansen 1996).

Twenty-seven core pieces were sealed in cans and analysed for their gas composition (Christiansen et al. 1997b; Dam et al. 1998). Sixteen of these are presented in Table 1 – the remaining nine samples had no detectable amounts of gas. Gas concentrations of the 16 samples were high, with significant amounts of wet gases such as propane, butane and pentane (Table 1). In some deeper parts of the well, concentrations were so high that the sampling cans deformed. Compositions in the deeper part are typical of thermogenic gas associated with oil (Table 1; Figs 5 and 7). Unfortunately, the isotopic composition trend suggests some diffusion after sampling as suggested by Christiansen et al. (1997b). The presence of a postmature oil-prone source rock in the deeper part (below 1100 m) of Umiivik-1 was documented in more detail by Drits et al. (2007).

4.7 GRO#3, drilled in 1996

GRO#3 was drilled by grønArctic Energy in the summer of 1996, following promising results from previous drilling and seep studies (Christiansen et al. 1997a, 1998).

Cores or sidewall cores were not included in the drilling programme, and the organic geochemical results are based on analysis of cuttings only (Bojesen-Koefoed et al. 1997b; Christiansen et al. 1998). Eight sandstone intervals were drillstem tested to obtain fluid samples, but results were inconclusive. Later, log interpretation indicated many intervals with high gas concentrations (Kristensen & Dam 1997). These petrophysical data are not presented in this review.

4.8 Vismann mineral exploration, drilled in 2007

The company Vismann Exploration Inc. drilled two mineral exploration boreholes in the Aaffarsuaq valley, in 2007, based on previously observed geophysical anomalies in the area (Fig. 2). The logistical operation was complex and required construction of a new road into the Aaffarsuaq valley. Both of the wells were suspended due to gas under pressure at depths of 154 and 133 m. Neither of the holes reached bedrock and they only penetrated the Quaternary overburden (glacial tills). Unfortunately, no gas was sampled.

4.9 Lakes and pingos

The best opportunity to observe gas seepage in land terrains, like the Nuussuaq Basin, is from lakes, pingos, below newly formed ice or on partly wet mud flats. Pingos are conspicuous mound-like landforms that are common in regions with continuous permafrost. They may have craters resembling those of mud volcanoes (Pissart 1988). Active pingos are formed by periglacial processes, have an ice core of frozen water and often grow over time. Some eventually collapse. Pingos are common in many valleys on Disko, Nuussuaq and Svartenhuk Halvø. Expedition anecdotes of bubbling lakes suggested the presence of gas seepage as early as the 1930s. Early analyses of both gas and water collected in the 1930s and 1940s were first presented in the context of petroleum exploration by Henderson (1969). These early analyses document a significant content of methane and alkaline water associated with gas seepage. Many of the pingos in the region were more systematically studied in the 1990s – most of them were dry. Some occasionally show crater lakes or outlets of spring water under artesian pressure. Sampling of these waters may give information on the composition of water and gases below the permafrost.

Pingo 132 (Fig. 2) north of the Aaffarsuaq river seems to have been rather active and wet over many decades. Note that Henderson (1969) uses the term Qapiortoq kitdleq for the same pingo. Pingo 132 was visited and sampled on several occasions in 1991 and 1992. Snow fans were observed to disappear from Pingo 132 later than on any other southward facing slopes in this part of the Aaffarsuaq valley. On one occasion, a fountain of water under pressure was observed (Fig. 8A). A similar feature was documented in a photo taken on 25 August 1939 by B. Thomsen (see fig. 6 in Henderson 1969).

Fig. 8 Features of Pingo 132 in Aaffarsuaq Valley, Gassø lake, and a new pingo near Marraat-1 core. A : Water fountain indicating water with a high gas content under artesian pressure below the permafrost, 17 August 1991. B : Surface of Gassø lake with clear indications of gas seepage, 28 July 1994. C : Doming, soil fracturing and possible formation of a new pingo near Marraat-1, 27 July 2006 (photo: Roy Fitzsimmons). D : Gas trapped under ice in a small pool near Marraat-1, 27 July 2006.

Looking downstream from the snow fan, which covers part of the pingo, the valley floor is described as being overgrown with algae and other vegetation, suggesting that the outlet has been active over long periods of the year and that the water is rich in nutrients. This remarkable colouration may be a good proxy for remote-sensing studies of other similar outlets in the region.

Elsewhere, gas seepage from the hinterland of Marraat is indicated by the so-called Gassø lake (Fig. 2), depicted in the 1:100 000 geological map of the area (Rosenkrantz et al. 1974) and the official Geodætisk Institut 1:250 000 topographical map from 1980. The lake was visited by Flemming G. Christiansen and Inger Salomonsen on 28 July 1994. The lake surface showed clear evidence of seepage as intense bubbling (Fig. 8B). Analyses of lake water (sampled in cans) indicated a complete dominance of nitrogen (Laier, unpublished data, October 1994; Supplementary File S2), suggesting either long-distance migration of gases that are thermally very mature, or more likely that oxygen had been lost by bacteria in an anoxic environment.

A third and more recent example is from the Marraat area, where a new pingo seems to be actively forming (Figs 2 and 8C). The normally flat riverbed surface is doming with new fractures in the peaty soil. The underlying ice-core is beginning to be exposed and large bubbles of gas are visible in small ponds nearby, beneath recently formed ice (Fig. 8D). Such features with fractures opening to permafrost below – and possibly with degrading permafrost – may become more common on Nuussuaq in the years to come, especially in areas with active movements.

4.10 Marine records

Geophysical data, including conventional seismic data and high-resolution shallow seismic data, indicate that gas could be very common in the sedimentary succession below the seabed of Vaigat (location in Fig. 2). Examples of so-called direct hydrocarbon indicators have been observed offshore in Vaigat, particularly as flat spots but also as gas cloud features (Bojesen-Koefoed et al. 2007).

Geochemistry data of pore waters from gravity cores indicate that gas hydrates may also be present at several places offshore in Disko Bugt and Vaigat (Mikkelsen et al. 2012; Nielsen et al. 2014). This is supported by numerous observations of pockmarks, seabed mud diapirs and change in reflection patterns on geophysical data in the area. Kuijpers et al. (2001) also observed intense degassing from two cores south of Disko. To the best of our knowledge, no gas samples have been analysed.

4.11 Summary: existing gas observations

Historical observations of gas seepage in the Nuussuaq Basin are to some degree supported by modern analytical data. Large parts of the Nuussuaq Basin are clearly underlain by a sedimentary succession that contains high concentrations of gas. Although dominated by biogenic gas, gases from surface lakes and pingos show a distinct thermogenic component. The gases from boreholes are mainly thermogenic in origin, and in some cases, their composition suggests an association with oil. These oil-associated gases have a rather low thermal maturity corresponding to the thermal maturity of the sediments penetrated by drilling.

In several cases, examples of thermally high-maturity gases have been recorded. These gases may have migrated from the deeper part of the sedimentary succession or were generated in the vicinity of dykes and sills. Clearly, better systematic sampling techniques, proper handling and storage, and most importantly, rapid analyses using modern instrumentation could provide much more valuable information.

GANT#1, Pingo 132 and the Vismann mineral exploration holes are all in close proximity to the anticline, suggested by Sørensen et al. (2017) to be a large potential target for future exploration. It is therefore particularly important to get more data on oil and gas seeps from this area.

5 2019 reconnaissance to sample oil and gas seepage

5.1 Biomarkers in oil seepage near the Kuugannguaq–Qunnilik Fault zone

On 26 July 2019, we visited a number of planned drill sites next to the Kuugannguaq–Qunnilik Fault zone in the Aaffarsuaq valley to check for oil seepage (Fig. 2). Hyaloclastites from the deep part of the Vaigat Formation were examined for signs of petroleum staining. The hyaloclastites are from unit 409 of the Nuusap Qaqqarsua Member within the Naujánguit Member of the Vaigat Formation (Fig. 3; see details in Pedersen et al. 2002, 2017). We sampled the hyaloclastites, located c. 340 m.a.s.l., close to the outlet of the Qunnillik canyon (sample site 574305 in Fig. 2), a few hundred metres west of the expected trace of the Kuugannguaq–Qunnillik Fault zone.

We picked out small pieces of a hard, fresh rock with thin carbonate veins and a distinct petroliferous odour for organic geochemical analyses using standard methods (Bojesen-Koefoed et al. 2018).

A sample of rock pieces was lightly crushed and extracted for 4 h (1 h immersed in boiling solvent followed by 3 h of rinsing) using a Soxhtec™ instrument and a 93+7 vol./vol. dichloromethane + methanol mixture as solvent. The extract was recovered by evaporation over N₂ and weighed. A 238 g sample was extracted to obtain a total yield of 6.2 mg extract, corresponding to c. 26 ppm. Asphaltenes were precipitated by the addition of 40-fold excess n-pentane. Asphaltenes were recovered by centrifugation and rinsed through several stages with n-pentane. Asphaltenes account for 27.4% by weight of the total. Maltene (i.e. asphaltene-free) fractions were separated in saturated hydrocarbons, aromatic hydrocarbons and polar fractions by medium-pressure liquid chromatography using a procedure modified from Radke et al. (1980). The maltene fraction is dominated by polar NSO compounds (Table 2).

Table 2 Maltene fraction extracted from oil-stained hyaloclastics (sample site 574305, Fig. 2) in the Affarsuaq valley, Nuussuaq Basin

Sample	Saturated hydrocarbons (wt.%)	Aromatic hydrocarbons (wt.%)	Polar compounds (wt.%)
574305	10.0	2.5	87.5
NSO: nitrogen, sulphur, oxygen.

The saturated hydrocarbon fraction was analysed by gas chromatography–flame ionization detection (GC_FID) using a Shimadzu gas chromatograph, furnished with a 30-m WCOT ZB-1 capillary column. Biomarker analysis was carried out by gas chromatography–mass spectrometry (GC–MS) using an Agilent 6890N gas chromatograph, fitted with a 30 m WCOT ZB-5 capillary column, coupled to a Waters (Micromass) Quattro Micro GC tandem quadrupole–hexapole–quadrupole MS. The instrument was run in both Selective Ion Monitoring mode (GC–MS_SIM) and GC–MS–MS parent–daughter mode. The sample was run several times using methods designed to optimise the representation of different compounds.

Gas chromatographic data on the saturated hydrocarbon fraction show a strongly front-end evaporated distribution of n-alkanes, a high proportion of long-chain components (Fig. 9A) and no unresolved complex mixture, suggesting limited biodegradation (Fig. 9A). Front-end losses of short-chain components make calculation of standard ratios futile, including the pristane/phytane ratio.

Fig. 9 GC FID and GC–MS–MS data (time vs. signal) for a sample of oil-stained hyaloclastics (sample site 574305; Fig. 2), Aaffarsuaq Valley, Nuussuaq Basin. A : GC FID data. B : GC–MS SIM for m / z 191. C : GC–MS–MS of pentacyclics. Sum of nine transitions. D : GC–MS–MS of steranes. Sum of five transitions. Symbols are as follows: nC x : normal alkanes ( x = carbon number); pristane : C 19 acyclic isoprenoid; phytane : C 20 acyclic isoprenoid; Ts : 18α-trisnorneohopane; Tm : 17α-trisnorhopane; H28 : 28,30-bisnorhopane; H29 : norhopane; 29ts : C 29 neohopane; M29 : normoretane; O+L : coelution of oleanane + lupane; H30 : hopane; M30 : moretane; HXX (S+R) : homohopanes, doublets 22S and 22R isomers; XX = carbon number; D27 : C27 diasteranes; S29 : C29 regular steranes; αααS : regular sterane ααα 20S isomer; αββS : regular sterane αββ 20S isomer; αββR : regular sterane αββ 20R isomer; αααR : regular sterane ααα 20R isomer.

The concentrations of tricylic terpanes (Fig. 9B) are relatively low, and their distribution partially obscured by the presence of abundant unknown components in the same range, probably various other tri- and tetracyclic components. Pentacyclic triterpanes show a series of hopanes ranging from C27 to C35, including notable proportions of 28.30-bisnorhopane (H28, Fig. 9C) and oleanane (O, Fig. 9C), plus trace amounts of bicadinanes and taraxastane (not shown). Extended 28-bisnorhopanes are absent, as are nor/bisnorlupanes. The bishomohopane isomerisation ratio has reached equilibrium at 0.61 (H32 S/(S+R), Table 3, Fig. 9C). The sample shows high concentrations of aromatic diterpanes which are a common feature of terrestrial oils found on Nuussuaq, moderate concentrations of phenanthrene and methylphenanthrene (not shown), and the presence of di- and triaromatic oleanane. The sterane distribution is strongly dominated by C29 moieties and shows very high proportions of diasteranes (Fig. 9D). C30 desmethyl steranes are absent, but C26-steranes are relatively prominent and allow calculation of a nordiacholestane ratio of 0.37 (Holba et al. 1998). C29-sterane 20S/(20S+20R) and αββ/(ααα+αββ) isomerisation ratios are both below equilibrium at 0.43 and 0.42, respectively (Table 3, Fig. 9D).

Table 3 Key geochemistry parameters for sample 574305

Sample	C19–26 Tricyclics/hopane	C23 Tricyclic/hopane	C25/C26 Tricyclics	C24 Tetracylic/hopane	H32 S/(S+R)	Ts/(Ts+Tm)	S29 S/(S+R)	S29 αββ/(ααα+αββ)
574305	0.09	0.01	0.83	0.01	0.61	0.41	0.43	0.42
H32 S/(S+R): bishomohopane isomerisation ratio; Ts/(Ts + Tm): 18α-trisnorneohopane/(18α-trisnorheohopane + 17α-trisnorhopane); S29 S/(S+R): C29 sterane 20S/(20S+20R) isomerisation ratio; S29 αββ/(ααα+αββ): C29 sterane αββ/(ααα+αββ) isomerisation ratio.

Sample 574305 can be classified as a “Niaqornarsuk type" oil with some notable deviations, according to its biological-marker characteristics as first defined by Bojesen-Koefoed et al. (1999; Table 4). A few parameters fall outside the established range for this oil type, notably the relative abundance of diasteranes and 28,30-bisnorhopane. However, the following diagnostic criteria are fulfilled:

Table 4 Comparison of sample 574305 with the Niaqornaarsuk oil type (Bojesen-Koefoed et al. 1999)

Sample		H28/H29	H29/H30	O/(O + H30)	D27/RS27	RS27/RS29	S27%	S28%	S29%
574305		0.31	1.14	0.18	4.0	0.32	19	21	60
Niaqornaarsuk oil type	Mean	0.17	0.92	0.06	0.87	0.32	20	14	65
	Minimum	0.13	0.81	0.04	0.73	0.20	15	12	57
	Maximum	0.23	1.02	0.10	1.19	0.47	27	17	73
H28/H29: 28,30-bisnorhopane to norhopane ratio; H29/H30: norhopane to hopane ratio; O/(O+H30): oleanane to oleanane + hopane ratio D27/RS27: C27 diasterane to C27 regular sterane ratio; RS27/RS29: C27 to C29 ratio of regular steranes; S27%, S28%, S29%: relative distribution of regular steranes.

1. Appreciable concentrations of 28,30-bisnorhopane and absence of extended 28-norhopanes (Table 4).
2. Presence of oleanane (perhaps coeluting with small amounts of lupane, see Nytoft et al. [2020]), with no or negligible concentrations of nor/bisnorlupanes (Table 4, Fig. 9C).
3. Strong predominance of C29-steranes and absence of C30 desmethyl steranes (Table 4, Fig. 9D).

The aromatic fingerprint, in particular the moderate concentrations of phenanthrene and methylphenanthrene, further supports the identification of sample 574305 as “Niaqornarsuk type" oil.

The characteristic features of the “Niaqornarsuk type" oil were originally defined using only GC–MS(_SIM) data, which are inferior to modern GC–MS–MS. Sterane data based on GC–MS(_SIM) suffer from coelution problems, which often cause misleadingly low ratios of diasteranes to regular steranes.

The Niaqornaarsuk oil type has been linked to Campanian-age source rocks, based on the geochemical correlation to Campanian-age shales of the GANT#1 borehole (Bojesen-Koefoed et al. 1999), which are perfectly conformable with a nordiacholestane ratio of 0.37 (Holba et al. 1998). The sample was collected at least 10 km from any other known occurrence of surface seepage near the Kuugannguaq–Qunnillik Fault zone, which is encouraging for future exploration. The presence of a Niaqornaarsuk oil type at a considerable distance from the only hitherto known occurrences of this oil type further supports the presumed existence of Campanian age deposits developed in source-rock facies in the region.

5.2 Gas seepage in Aaffarsuaq Valley

5.2.1 Remote-sensing analysis of Pingo 132

On 26 July 2019, Pingo 132 in the Aaffarsuaq valley, central Nuussuaq, was visited to check for mud extrusion and gas seepage (Fig. 2). Although Pingo 132 is periglacial in origin, it resembles typical mud volcanos from classical petroliferous basins or geothermal fields with mud overflow (see Etiope 2015; Mazzini & Etiope 2017; Mazzini et al. 2011).

Today, there is evidence of recent mud extrusion in the area. The mud cropping out is pale in colour, has rather steep sides and many irregular fractures and erosional features that are not likely to survive more than a few winters. There is little to no vegetation on the extruded mudstone, which is in contrast to the older parts of the pingo and surrounding valley floor. The actual mudstone contains numerous clasts of rounded basements boulders, some Cretaceous Atane Formation sandstone lithologies and a few volcanic rock types – all typical of the Quaternary tills in the Aaffarsuaq valley (Fig. 10).

Fig. 10 Extruding muds from the side of Pingo 132. Note the many rounded basements boulders in the mud. Height of section c . 3 m. Photo taken on 26 July 2019.

High-resolution satellite images provide good possibilities for detecting surface movements of the pingo and measuring slow displacement rates of centimetres to metres per year. Using Differential Synthetic Aperture Radar (SAR) interferometry (DInSAR; Rosen et al. 2000) to plot the phase differences between two or more satellite SAR images allows us to detect movement in the direction of line-of-sight of a few millimetres and helps characterise the dynamics of terrain uplift. Combining the two complementary techniques overcomes the limitations of using just one of these methods.

To visually identify the changes in the shape of Pingo 132 and outcropping mud over time, we used optical four-band PlanetScope time-series with 5 m spatial resolution between 2017 and 2019 (Fig. 11A). The Normalized Difference Vegetation Index (NDVI) is calculated from the same dataset (Fig. 11B) to enhance the interpretation of the identified patterns and to measure the concentration of green vegetation. Two Sentinel-1 tracks (i.e. 171 descending and track 90 ascending) cover the same area. Differential SAR Interferometry was carried out for the descending track between 11 June and 3 September 2019 using the Arctic digital elevation model (Porter et al. 2018). The interferograms were unwrapped, and the deformational rates are reported as the satellite line-of-sight rates projected onto the steepest slope. The results indicate significant vertical movements in both summer and winter, suggesting “uplift" rates of c. 1 cm every 12 days, probably related to mud accumulation (Fig. 11C). Furthermore, seasonal variation in the uplift rate seen in the DInSAR data matches the seasonal pattern observed in the optical data. It seems that most of the observed mud extrusion took place in the summer of 2017.

Fig. 11 Remote-sensing images and analysis of Pingo 132, Affarsuaqq valley. Red-dashed lines indicate the location of Pingo 132. A : Optical four-band PlanetScope data with 5 m spatial resolution for July and August 2017–2019. B : Normalized Vegetation Index (NDVI) for July and August 2017 and 2019. Negative values of NDVI correspond to water. Values close to zero (–0.1 to 0.1) generally correspond to barren areas of rock, sand or snow. Low positive values (0.2–0.4) represent shrubs, while high values (approaching 1) indicate green vegetation. C : Close-up of Pingo 132. Selected differential interferograms (wrapped interferometric phase) from track 175. Upper row: 10 August 2019–22 August 2019 (temporal baseline: 12 days; normal baseline: –0.06 m). Lower row: 5 July 2019–17 July 2019 (temporal baseline: 6 days; normal baseline: 15.68 m) and 11 June 2019–23 June 2019 (temporal baseline: 6 days; normal baseline: 5.46 m).

5.2.2 Geochemistry of gas seepage

The present water outlet is on the lower, south side of the pingo. It is associated with fractures in the soil and peat and small ponds with bubbling gas (see videos in Supplementary Files S4 and S5). Some of the partly dry mudflats show gas-escape vents (Fig. 12A). The sandier material displays a crater-like feature, a few centimetres in size (Fig. 12B).

Fig. 12 Gas seepage from Pingo 132. A : Gas escape structures on recently dried-out mud flat on the southern side of Pingo 132, 26 July 2019. Size is c . 20 × 30 cm. B : Centimetre-scale mounds formed by gas seepage at Pingo 132, 26 July 2019. Hammerhead for scale.

A gas sample was taken in a plastic bottle where gas displaced the outlet water, kept cool and analysed within a week for CH₄ and C₂H₆ by standard gas chromatography (Christiansen et al. 1997b). The sample was stored and later analysed for stable carbon and hydrogen isotopes by Martin Krüger at Bundesanstalt für Geowissenschaften und Rohstoffe in Hannover (for methods, see Blumenberg et al. 2016). The seeping gas is mainly composed of methane with a small amount of ethane (Table 5). The carbon isotope composition of methane and ethane using standard classification plots suggests a thermogenic origin with a relatively low thermal maturity (Figs 5–7).

Table 5 Geochemistry of gas escaping from Pingo 132 sampled in 1991, 1992 and 2019

Sample number	Date	CH4 (C1) (ppm)	C2H6 (C2) (ppm)	δ13C1 (‰)	δ13C2 (‰)	δDC1 (‰)	Wetness	Data sources
358472	17 August 1991	723 000	530	−45.8	n.a.	n.a.	1364	Laier 1994
400843	14 July 1992	468 000	n.d.	−40.4	n.a.	n.a.	n.d.	Laier 1994
400844	14 July 1992	81 800	790	−38.1	n.a.	n.a.	1035	Laier 1994
400894	14 August 1992	355 000	175	−43.4	n.a.	n.a.	2028	Laier 1994
547303	26 July 2019	239 000	164	−43.2	−34.5	−233	1460	This study
n.a.: not analysed; n.d.: not determined. Wetness: C1/(C2 + C3). C3 not present in any samples.

5.2.3 Geochemistry of water associated with gas accumulation or seepage

Geochemistry of formation water associated with oil and gas accumulations or related to oil and gas seepage may provide important additional information on the migration and degradation history. Water under pressure has been recorded in a few places on Nuussuaq, both in the Marraat-1 and GANK#1 wells and in some pingos. Some historical data were published by Henderson (1969), and additional data from the early nineties were compiled and reported by Christiansen et al. (1995b). These are presented in Table 5 along with new data for Pingo 132.

The formation fluids from Marraat-1 have a higher salinity than seawater and a very high Ca/Mg ratio suggesting a deep brine origin (Table 6). There is some variation between different levels, suggesting that the different volcanic lithologies and their content of zeolites could affect composition.

Table 6 Geochemistry of water samples from Pingo 132 and nearby formation water, seawater and river water

Sample	Location	Type	pH	Alk	Cl (mg/l)	SO4 (mg/l)	Na (mg/l)	K (mg/l)	Ca (mg/l)	Mg	Cl/SO4	Na/K	Ca/Mg	Data sources
358472	Pingo 132	Fountain water	8.78	46.6	256	200	1135	9.48	3.68	86	1.28	119.7	0.04	Laier 1994; Christiansen et al. 1995b
400843	Pingo 132	Fountain water	8.97	42.6	248	178	1110	9.74	1.68	68.5	1.39	114.0	0.02	Laier 1994; Christiansen et al. 1995b
400844	Pingo 132	Fountain water	8.97	29.7	53.1	177	750	6.72	2.46	54.5	0.30	111.6	0.05	Laier 1994; Christiansen et al. 1995b
400894	Pingo 132	Fountain water	8.78	44.8	258	180	1140	9.28	2.63	76.5	1.43	122.8	0.03	Laier 1994; Christiansen et al. 1995b
547303	Pingo 132	Fountain water	7.87	3.17	19.9	2.16	69.6	1.52	4.30	5.71	9.2	45.7	0.75	This study
408011	Marraat-1	Formation water (41 m depth)	7.42	0.92	29 200	1484	9650	188	6740	790	19.68	51.3	8.53	Laier 1994; Christiansen et al. 1995b
408021	Marraat-1	Formation water (82 m depth)	7.41	0.58	29 600	1252	8180	126	8560	630	23.64	64.9	13.59	Laier 1994; Christiansen et al. 1995b
408035	Marraat-1	Water under pressure (346 m depth)	7.15	0.43	26 500	1276	6780	167	8160	630	20.77	40.6	12.95	Laier 1994; Christiansen et al. 1995b
408036	Vaigat, Maraat-1	Sea water	7.94	2.10	19 500	2340	10 500	402	430	1230	8.33	25.2	0.36	Laier 1994; Christiansen et al. 1995b
380132	Vaigat, GANW#1	Sea water	7.94	2.20	18 930	2033	8797	403	412	1217	9.31	21.8	0.34	Laier 1994; Christiansen et al. 1995b
380133	GANW#1	River water	8.20	3.20	13	11	20.7	0.29	32.4	17.5	1.18	71.4	1.85	Laier 1994; Christiansen et al. 1995b
Alk: alkalinity.

Pingo 132 is less saline than Marraat-1 (Table 6). It should be noted that in Pingo 132, there is an increased salinity compared to river water, and with high Na/K ratios, low Ca/Mg ratios and low Cl/SO₄ ratios (Table 6). The 1991 and 1992 samples (fountain water only) have a rather consistent composition through time and a slightly enriched pH between 8.78 and 8.97 (average: 8.89) compared to the river, sea and formation waters and a high alkalinity (Table 6). The 2019 sample was collected in a small pool and seems to be dominated by surface water from melting snow.

6 Implications for exploration and recommendation for future studies

The 2019 and previously documented gas data and 2019 oil seep data from Nuussuaq support an exploration model for the anticlinal structures mapped by Sørensen et al. (2017). Petroleum extracted from an oil-stained hyaloclastite sample, collected in the Aaffarsuaq valley, in 2019 represents a facies variety of the “Niaqornaarsuk type" sensu Bojesen-Koefoed et al. (1999). The presence of a “Niaqornaarsuk type" oil 10 km from other known occurrences of this oil type further supports the presumed existence of Campanian age deposits developed in source-rock facies in the region. Importantly, we observed no sign of mixing with the “Marraat type," suggesting that the Marraat source rock disappears somewhere between GANK#1 and the Kuugannguaq–Qunnilik Fault zone, or that the source rock, if present, is thermally immature. Furthermore, numerous examples of gas occur within a few kilometres on either side of the mapped anticline and along possible migration pathways. These gases have a thermogenic fingerprint and suggest a possible origin from oil-prone source rocks with a relatively low thermal maturity.

Further geological and structural mapping using 3D photogrammetry combined with geophysical data would be an ideal approach to develop the exploration model in the region. Moreover, future studies should systematically sample oil traces along faults and fractures and focus on rock types with carbonate-filled veins that often host fluid inclusions, to elucidate the vertical and lateral distribution of the active petroleum systems in the Nuussuaq Basin. In some ways, this compares to the practice of traditional onshore exploration in areas like California and Texas more than a hundred years ago, where targets were often defined by a combination of surface structures and seeps. This rule of thumb is still valid in many onshore areas around the world, but knowledge of the distinct oil types can guide exploration even more efficiently.

Systematic mapping, sampling and characterisation of gas seepage from pingos, lakes and thawing permafrost could be similarly important in the future. Professional sampling tools for both onshore and offshore activities, including transport and storage of samples under cool conditions, are important, and samples should be analysed as soon as possible to reduce contamination and diffusion. Modern isotope techniques with better resolution and low detection limits are likely to provide more details compared to the preliminary work of the 1990s. With degrading permafrost and some specific pingos experiencing rapid change, many more sampling sites are likely to be identified. Based on Pingo 132, it is obvious that satellite data providing both optimal images and interferograms can systematically identify areas of degrading permafrost. This would allow us to identify suitable sites to collect samples of gas and water that originate from below the permafrost seal. Furthermore, satellite data can be used for preliminary dating of mud extrusions.

Finally, it must be emphasised that the changes observed over the last decades and years point towards a dynamic situation caused by climate change. This may potentially lead to much more frequent mud diapirism and emissions of gas in large parts of the Nuussuaq Basin when more permafrost degrades in the future. There is a strong need for many of the localities to be documented and monitored in detail. This has implications not only for petroleum exploration but also from a viewpoint of nature preservation as many new local ecosystems are likely to develop and change over time in the coming decades.

Acknowledgements

Analytical data are from many different field projects by GGU/GEUS with additional funding from Danish and Greenlandic authorities. Contributions came especially from the former Danish Ministry of Energy Research Program (EFP), the previous Mineral Resources Administration for Greenland in Copenhagen, the previous Bureau of Minerals and Petroleum in Nuuk and recently from the present Ministry of Industry, Energy, Research and Labour, Nuuk, Greenland. Close collaboration with industry over the years, especially grønArctic Energy Inc. and its enthusiastic manager Cam Hanna has been very useful. Practical help over many years and analytical support by John Boserup, Ditte Kiel-Duhring, H. P. Nytoft and Christina Rosenberg Lynge are highly appreciated. Martin Krüger at Bundesanstalt für Geowissenschaften und Rohstoffe in Hannover is gratefully acknowledged for performing isotopic analyses of the pingo gas samples collected in 2019. We would like to thank Dietmar Backes from the University of Luxembourg for giving us access to PlanetScope imagery provided via the Planet’s Education and Research program that has been used for generation of NDVI maps. Comments on the paper by the reviewers Chris Parry and Sverre E. Ohm were welcome.

Additional information

Author contribution

FGC: writing the original draft (lead). JABK: analyses, presentation and discussion of oil geochemistry data. GD: contribution to historical data and petroleum exploration model. TL: analyses, presentation and discussion of water and gas geochemistry data. SS: analyses, presentation and discussion of satellite data.

Additional files

Six additional files are available online: https://doi.org/10.22008/FK2/SO5VLD.

References

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