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Assessment of the hydrocarbon potentiality of the Late Jurassic formations of NW Iraq: A case study based on TOC and Rock-Eval pyrolysis in selected oil-wells

  • Swar J. Al-Atroshi EMAIL logo , Govand H. Sherwani and Srood F. Al-Naqshbandi
Published/Copyright: December 18, 2019
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Open Geosciences
From the journal Open Geosciences Volume 11 Issue 1

Abstract

The Late Jurassic Naokelekan and Barsarin formations of northwestern Iraq have been investigated in three wells to assess their potentiality for hydrocarbon generation.

The results of Total Organic Carbon content (TOC) and Rock-Eval Pyrolysis reveal fair to excellent content of hydrocarbon and suggest that the depositional conditions were suitable for the production and preservation of organic matter. The Thermal Maturity Proxy indicates that the studied formations were mature stage of hydrocarbon generation, with an exception of three samples from the Naokelekan Formation in Shaikhan-8 well, and two samples from the Barsarin Formation in Atrush-1 and Shaikhan-8 wells were at an immature stage.

The S1 and TOC relationship shows that all the samples are indigenous in nature. Most of samples from the Naokelekan Formation belong to kerogen Type II/III, and that in the Barsarin Formation belongs to kerogen Type II is dominant.

The Pr/Ph, Pr/n-C17 and Ph/n-C18 ratios for the extracted bitumen of both the formations indicate that they were originated from marine organic matter under reducing conditions. The δ13CSat and δ13CAro range from −28.7 to −27.7‰ and −28.8 to −27.7‰ respectively. These biomarkers show high contribution of marine organic matters preserved under relatively anoxic conditions in the studied formations.

Keywords: Naokelekan Fm.; Barsarin Fm.; Mangesh; Atrush; Shaikhan; Rock-Eval; Biomarker

1 Introduction

Many hydrocarbon fields have been discovered in deeper Jurassic reservoirs of the northwestern part of Iraq in the recent years, such as Tawki, Atrush, Swara Tika and Shaikhan fields. The Jurassic period represents a separate and distinct petroleum systems much distinct from those of the Triassic systems, in that they their independent internal source rocks, reservoirs, and regional seals [1, 2].

Atrush and Shaikhan oil fields are located in the High Folded Zone which is part of the Zagros Fold and Thrust Belt of Iraq, some 85 km northwest and 60 km north of Erbil city respectively. Both are recent oil discoveries in the Kurdistan Region of Iraq. The Atrush structure is a NW-SE oriented, doubly-plunged asymmetrical anticline, and its northeastern limb is gentler than the southwestern one. The dip of the steeper forelimb may reach > 70∘, and is overturned in some localities [3].

The Shaikhan anticline is a WNW-ESE trending, doubly-plunged asymmetrical anticline with a gentle southwestern limb and steeper backlimb. Consequently, this anticline is verging towards the northeast (hinterland). Furthermore, the attitude of the fold axis is 275∘/5∘, and the anticline is plunging 5∘ towards WNW. This fold is considered as an open structure due to its interlimb angle of 120∘ [4].

The Late Jurassic Naokelekan and Barsarin formations were first described by [5] from outcrops in the Balambo-Tanjero Zone at Naokelekan and Barsarin Villages in NE Iraq. The Naokelekan Formation conformably overlies the Sargelu Formation [6], and its upper contact with the Barsarin Formation is frequently marked by a detrital, ferruginous horizon in north Trust Zone [7]. The upper contact of Barsarin Formation with Chia Gara is conformable in the type area [5].

The Upper Callovian-Lower Oxfordian, with Kimeridgian and Oxfordian ages were suggested for Naokelekan and Barsarin source rocks in North Iraq respectively [8]. This was based on the study of Palynomorphs, mainly dinoflagellate cysts. Whereas, the age of Naokelekan Formation in Iraqi Kurdistan was indicated as Callovian to Upper Oxfordian based on the presence of Cyclagelosphaera deflandrei sp. and lotharingius sp. [9]. The amount of Total Organic Carbon (TOC) of the Naokelekan Formation decreases toward west, north, and southeastern parts of Iraqi Kurdistan ranging between 0.4 to 18.8 wt.%, [10] and that the types II and III kerogens are the main components of organic matter [10, 11].

This study is the first one conducted on Mangesh-1 (Ma-1), Atrush-1 (At-1) and Shaikhan-8 (Sh-8)wells (Figure 1). Although Naokelekan and Barsarin formations are consider as important sources of hydrocarbons in the northern Iraq basins, there are lack subsurface studies on the formations in northwestern Iraq. The objective being assessment of the TOC content and kerogen type characterization, along with determination of its maturity stage in order to deduce the genetic potential (GP). Furthermore, the depositional conditions of Late Jurassic Naokelekan and Barsarin formations are being studied by integrating organic geochemical data and molecular characterization.

Figure 1 Landsat image showing the locations of the studied wells, Ma-1, At-1 and Sh-8
Figure 1

Landsat image showing the locations of the studied wells, Ma-1, At-1 and Sh-8

2 Geological Setting of Late Jurassic Period/Formations

The Jurassic period in Iraq invariably includes the Late Toarcian-Early Tithonian Megasequence (AP7) spatially and temporally. There are several genetically related sequence packages that were deposited during this period.

The geological successions exposed within the studied well-sections include Jurassic Alan, Sargelu, Naokelekan and Barsarin formations from the oldest to youngest. Younger Cretaceous units are comprised of Chia Gara, Garagu, Sarmord, Qamchuqa, Kometan,Wajna, and Aqra formations. These were further overlain by the Tertiary succession comprised of Kolosh, Gercus and Pila Spi formations (Figure 2).

Figure 2 Stratigraphic column of Sh-8 well with a summary of lithology
Figure 2

Stratigraphic column of Sh-8 well with a summary of lithology

Naokelekan Formation overlies Sargelu Formation and the represented contact between them is conformable [5]. The upper contact, of which is also conformable with the Barsarin Formation, is frequently marked by a detrital, ferruginous horizon in north Thrust Zone [7].

The lithology of Naokelekan Formation from bottom to top in the studied wells consists of:

  1. Argillaceous limestone, light to medium to dark grey, occasionally brownish grey, firm blocky, hard in part, subangular to angular, brittle, microcrystalline, slightly dolomitic.

  2. Pale grey-brown limestone, rarely dark grey-brown, hard, brittle, sub-blocky to angular microcrystalline, argillaceous in part, slightly dolomitic.

  3. Calcareous claystone, which is very dark grey to brownish grey, rarely black, moderately hard, sub-blocky to angular, carbonaceous (Figure 3).

Figure 3 Lithologic description of the studied formations in Ma-1, At-1 and Sh-8 wells
Figure 3

Lithologic description of the studied formations in Ma-1, At-1 and Sh-8 wells

Barsarin Formation conformably overlies Naokelekan Formation and conformably underlies Chia Gara Formation in the type area [5] and the studied wells.

The lithologic composition of Barsarin Formation from bottom to top in the studied wells, consists of:

  1. Snowy white anhydrite, soft occasionally firm.

  2. Limestone, medium to dark brown in color, moderately to very hard, brittle, blocky to angular, firm to moderately hard, blocky, crumbly, slightly argillaceous.

  3. Shale, light grey to dark grey, brownish, moderate soft to moderate hard, fragile and fissile.

  4. Claystone, predominantly light grey, soft, amorphous, occasionally grading medium grey, moderately hard.

  5. Dolomite, medium to dark brown in color, hard, brittle, blocky to angular (Figure 3).

The area of the High Folded Zone of Iraq including, Balambo-Tanjero and Northern Thrust Zones is characterized by condensed sedimentary successions of euxinic environment in the lower part (Naokelekan Formation), and lagoonal evaporites in the upper part (Barsarin Formation). This in turn led [12] to confer the presence of a tectonic ridge separating the basin in northern Iraq.

The available palaeogeographic maps for Late Jurassic demonstrate that the entire area was influenced by tectonic load along the Arabian Plate margin prior to the opening of the southern Neo-Tethys. Compartmentalization of intra- shelf basin subsidence caused the basin break up and split from Neo-Tethys [1]. Three main types of prominent facies along with their depositional environments are recognized: (1) a clastic-carbonate amalgamation setting, is indicative of the inner carbonate shelf (submerged ridge), represented by the Najmah and Saggar formations; (2) a carbonate-evaporite setting, is indicative for inner shelf (sabkha), represented by the Najmah and Gotnia formations; and (3) a restricted basin setting, denoted by the Naokelekan, Barsarin and Gotnia formations (Figure 4).

Figure 4 Palaeogeographic map of Late Jurassic period (modified after [1])
Figure 4

Palaeogeographic map of Late Jurassic period (modified after [1])

A large-scale intrashelf basin, termed Gotnia Basin, was formed in Iraq at the end of Early Jurassic. This basin occupied most of the southern, central, northern and northeastern Iraq and was relatively isolated from the open-marine waters of Tethys. It was highly restricted in Mid- to Late-Jurassic period, resulting in the deposition of rich source rocks and evaporites. The margins of the basin were probably controlled by a system of conjugate NW-SE and SW-NE trending lineaments [2].

3 Sampling and Analytical Techniques

A total of 15 well cutting samples were collected from shale and bituminous limestones within the Naokelekan and Barsarin formations (Table 1). All the samples were analyzed at the Geological Survey Repository Facility in Erbil-Iraq.

Table 1

Details of the cutting samples collected from Naokelekan and Barsarin formations in Iraqi Kurdistan for Rock-Eval pyrolysis

Well nameFormationsNumber of samplesFormation thickness (m)Deposition (Ma)|
Ma-1Barsarin3138153-146
Naokelekan492164-153
At-1Barsarin277153-146
Naokelekan17164-153
Sh-8Barsarin251153-146
Naokelekan334164-153

The TOC (wt.%) was determined using a Buchner funnel and LECO C230 analyzer. The studied rocks were analyzed by Rock Eval pyrolysis method which estimates the GP (GP=S1+S2, in Kg HC/Ton rock) of rock samples using Rock-Eval 6 apparatus, according to a programmed temperature pattern. This was followed by heating the samples to 850∘C at rate of 25∘C/min in an oxidation oven in the presence of air to oxidize the residual carbon [13, 14]. The released hydrocarbons were monitored by Flame Ionization Detector (FID), generating two distinct peaks, S1 (thermally distilled free hydrocarbons in mg HC/g of rock) and S2 (hydrocarbons released from the cracking of kerogen in mg HC/g of rock). In addition, carbon dioxide (CO2) released during pyrolysis was monitored in real time by IR cell S3 (in mg CO2/g of rock), giving information on the oxidation state of the kerogen. The temperature at the S2 peaks is called (Tmax in ∘C), which gives an indication of kerogen maturity. Tmax can also be used to calculate Vitrinite Reflectance (Ro) which is mathematically expressed by [15] as Ro(calculated) = (0.018×Tmax) − 7.16

Other diagnostic ratios have been calculated from the S1, S2, S3 and TOC such as Production Index (PI=S1/GP), Hydrogen Index (HI=S2/TOC×100, in mg HC/g TOC) and Oxygen Index (OI= S3/TOC×100, in mg CO2/g TOC). Pyrolysis data were recorded with an aim to characterize the organic richness, kerogen type, petroleum generation potentiality and their thermal maturity [13, 14, 16, 17].

Gas chromatography (GC) was prepared to measure the abundance of alkane peak introduced by syringe into capillary column pursued by ionization during a controlled period. Six rock extracts were fractionated and analyzed in a similar fashion to the oils using Hewlett Packard HP 6890 Series II GC gas chromatograph. Stable carbon isotopic composition of the saturate and aromatic hydrocarbon fractions was determined, and the branched/cyclic fractions were analyzed by GC and Gas chromatography-Mass Spectrometry (GC-MS).

The samples of Naokelekan and Barsarin formations in the three studied wells were performed by StratoChem Cervices, New Maadi Cairo, Egypt.

4 Results and Discussion

4.1 Hydrocarbon potential

The hydrocarbon potential of Naokelekan and Barsarin formations in Ma-1, At-1 and Sh-8 wells was determined from Rock Eval data (Table 2). Several parameters were examined for extracting the thermal maturity of the possible source rocks. Quality of organic matter (OM) determines whether the kerogen is oil-prone (Type I and II) or gas-prone (Type III), [14].

Table 2

Results of Rock-Eval pyrolysis for the samples from Ma-1, Atr-1 and Sh-8 wells

Well nameFormationDepth (m)TOC Wt.%S1S2S3Tmax ∘CHIOIPIGPRo %
Ma-1Barsarin23191.491.066.920.61430464410.137.980.58
Barsarin23970.980.622.400.58437245590.213.020.71
Barsarin244813.003.1452.480.8044240460.0655.620.8
Naokelekan24636.072.1122.090.90437364150.0924.20.71
Naokelekan24841.100.543.940.64436358580.124.480.69
Naokelekan25021.050.363.020.93433288890.113.380.63
Naokelekan25440.520.281.590.544343061040.151.870.65
At-1Barsarin11600.780.903.970.32427512410.184.870.53
Barsarin11801.590.878.060.42433507260.108.930.63
Naokelekan12101.571.007.860.38432501240.118.860.62
Sh-8Barsarin14953.131.2216.701.03429534330.0717.920.56
Barsarin15092.361.3312.990.70434550300.0914.320.65
Naokelekan15420.900.252.081.044272321160.112.330.53
Naokelekan15571.180.243.330.91429282770.073.570.56
Naokelekan15691.240.363.891.254283141010.084.250.54

The S1 versus TOC plot provides the conclusive evidence about the origin of hydrocarbon present, whether it is indigenous (autochthonous) or non-indigenous (allochthonous), [18]. Figure 5 elucidates that all the analyzed samples from Ma-1, At-1 and Sh-8 wells lie below the inclined line (not migrated), and most of them have high TOC relative to low S1 values, indicating their indigenous origin and free from contamination.

Figure 5 Plot of Total Organic Carbon (TOC) versus S1 for the identification of migrated hydrocarbons of Naokelekan and Barsarin formations samples
Figure 5

Plot of Total Organic Carbon (TOC) versus S1 for the identification of migrated hydrocarbons of Naokelekan and Barsarin formations samples

The measured Tmax values ranging between 427∘C and 442∘C indicate that all the samples were thermally maturated early [19]. Similarly, the OI values ranging from 6 to 166 mg CO2/g rock, are < 200 mg CO2/g rock, which indicates that there is no intensive weathering or mineral decomposition in analyzed rock samples [20]. Calculated Ro values ranging between 0.53 and 0.80%, corresponds to the onset of oil generation (Table 2).

The pyrolysis data (HI vs Tmax) indicates that most of the analyzed samples from the Naokelekan Formation are limited to the mature and immature zones of mixed Type II–III, whereas most of samples from the Barsarin Formation fall within the mature field of kerogen Type II (Figure 6). This also corresponds to their HI and Tmax values that range from 245 to 550 mg HC/g TOC, and 427 to 442∘C respectively (Table 2). This suggests that the Naokelekan Formation in Ma-1 and At-1 wells are more likely to be gas prone, while Barsarin Formation in the same wells have limited capacity to generate liquid hydrocarbons.

Figure 6 Plot of Hydrogen Index (HI) versus (Tmax) for the analysis of samples of Naokelekan and Barsarin formations
Figure 6

Plot of Hydrogen Index (HI) versus (Tmax) for the analysis of samples of Naokelekan and Barsarin formations

TOC content of the studied samples ranges from 0.52 to 6.07 wt% and 0.78 to 13.00 wt% with an average of 1.7 wt% and 3.3 wt% for the Naokelekan and Barsarin formations, respectively, indicating fair to excellent organic-richness (Table 2). The variation in TOC of Naokelekan and Barsarin formations from one well to another are due to the change of the environmental conditions that produced different lithologies. A number of samples from the Naokelekan Formation are rated in TOC higher than the rating depending on S2, probably due to some oxidized and/or reworked OM within different depositional environments (Figure 7).

Figure 7 Plot of Pyrolysis S2 versus Total Organic Carbon (TOC) showing generative source rock potential of Naokelekan and Barsarin formations
Figure 7

Plot of Pyrolysis S2 versus Total Organic Carbon (TOC) showing generative source rock potential of Naokelekan and Barsarin formations

A plot of S2 versus TOC demonstrates that most samples from both formations are Type II, Kerogen and prone to different levels of oil and gas (Figure 8). These results were supported by the previous work that performed by [21].

Figure 8 Plot of Total Organic Carbon (TOC) versus pyrolysis S2 shows the kerogen type for samples from Naokelekan and Barsarin formations. It also indicates whether the kerogen is oil or gas prone
Figure 8

Plot of Total Organic Carbon (TOC) versus pyrolysis S2 shows the kerogen type for samples from Naokelekan and Barsarin formations. It also indicates whether the kerogen is oil or gas prone

4.2 Gas chromatographic analysis

Six cutting samples from Naokelekan and Barsarin formations were chosen belonging to Ma-1, At-1 and Sh-8 wells to carry out the geochemical parameters of isoprenoid hydrocarbons, i.e., pristane (Pr) and phytane (Ph), that could act as indicators of the depositional environments (Table 3). Carbonate source rocks which were deposited in a reduced or anoxic depositional environment have <2 Pr/Ph value [15]. The higher Ph content and lower Pr/Ph ratio is

Table 3

Gas Chromatograph/Mass Spectrometry coupled with Isotope data of Naokelekan and Barsarin formations cutting samples

Well nameFormationDepth (m)δSat13‰δAro13‰CVPr/PhPr/n- C17Ph/n- C18CPIC27%C28%C29%
Ma-1Barsarin23970.870.160.240.96
Naokelekan2484−27.9−27.7−2.550.820.240.300.9753.214.732.1
At-1Barsarin1160−28.7−28.8−2.980.320.400.950.9133.716.449.9
Naokelekan1210−28.6−28.2−1.890.370.340.720.9254.516.029.5
Sh-8Barsarin1509−28.3−28.0−2.210.440.330.561.0449.915.434.7
Naokelekan1569−27.7−27.7−3.061.040.320.361.2856.615.228.2

  1. δ13CSat‰=Stable carbon isotopic composition of the saturated HC fraction; δ13CAro‰=Stable carbon isotopic composition of the aromatic HC fraction; C27%=100×C27R/(C27R+C28R+C29R); C28%= 100×C28R/(C27R+C28R+C29R); C29%= 100×C29R/(C27R+C28R+C29R) whereas those of oils were invariably <1.2 [23]. e.g., mature source rocks have CPI values of 0.8<CPI<1.2, [19].

possibly due to the reducing environment at the time of the deposition of the source rock [22].

The Carbon Preference Index (CPI) is used as an indicator for maturity [15] CPI = 2(C23+C25+C27+C29) / [C22 + 2(C24+C26+ C28) + C30]. Early researches maintained that immature source rocks often had high CPI values of >1.5,

The Naokelekan and Barsarin formations in the three wells have low Pr/Ph values of (0.37-1.04) and (0.32-0.87) respectively, indicating an anoxic, reduced marine carbonate depositional environment [24], (Figure 9). This conclusion has been noted by [25] at Miran-2 well, Miran oil field, NE Iraq. The Pr/n-C17 ratio is helpful for discriminating OM that formed under marine environment <0.5, from those formed in swamp environment >1.0, [26]. Lower values of Ph/n-C17, and Pr/n-C18 indicate marine source rock bearing Type-II kerogen [27].

Figure 9 Gas chromatographs of extracted rock samples from Naokelekan (A,C,E) and Barsarin (B,D,F) formations, NW Iraqi-Kurdistan
Figure 9

Gas chromatographs of extracted rock samples from Naokelekan (A,C,E) and Barsarin (B,D,F) formations, NW Iraqi-Kurdistan

The Pr/n-C17, Ph/n-C18 ratios of the six extract samples for the Naokelekan and Barsarin formations are 0.24–0.34; 0.30–0.72 and 0.16–0.40; 0.24–0.95, respectively (Table 3), indicating that the extracted bitumens were derived from a carbonate-rich-source rock, deposited in an anoxic marine environment and also appear to be medium to low biodegraded (Figure 10). The CPI of the extracts of both studied formations are >0.80 and <1.20 indicating marine source at the maturation stage, albeit with an exception of Naokelekan Formation sample in Sh-8 well with CPI value of 1.28 indicating immature stage (Table 3).

Figure 10 Pr/n-C17 versus Ph/n-C18 of extracts from Naokelekan and Barsarin formations in the studied wells
Figure 10

Pr/n-C17 versus Ph/n-C18 of extracts from Naokelekan and Barsarin formations in the studied wells

4.3 Carbon isotopes composition (δ13C‰)

The isotope composition of the extracted bitumen (saturates and aromatics) can be used to distinguish between terrigenous and marine depositional environments by applying a mathematical relation known as Canonical Variable (CV) given by [28], stated as, CV = −2.53δ13CSat + 2.22δ13CAro −11.65. The CV value of > 0.47 mostly indicates terrigenous organic matter, whereas < 0.47 indicates predominantly marine organic source [28]. The calculated CV for the studied extracts ranges from - 3.06 to - 1.89 indicating prevalent marine environment (Table 3).

On the other hand, values of carbon isotope for the saturates (δ13CSat) and aromatics (δ13CAro) for five rock extract samples, belonging to Naokelekan and Barsarin formations, range from −28.7 to −27.7‰ and −28.8 to −27.7‰, respectively (Table 3). These values indicate a slight variation in isotopic composition of the extracted samples, owing to the maturation level between them [29]. It indicates that the OM of these formations was mainly derived from the marine source (Figure 11).

Figure 11 δ13C saturate versus δ13C aromatic cross plot for the analyzed extracts
Figure 11

δ13C saturate versus δ13C aromatic cross plot for the analyzed extracts

The GC-MS method was applied to monitor the ions with a mass/charge (m/z) ratio of 191 (terpanes) and 217 (steranes). Steranes are derived from sterols which are widely diffused in plants and microorganisms. The C27 and C28 sterols are most abundant in marine organisms and the C29 sterols in higher plants (Table 3). These general distributions in rock extracts can be used to indicate biological origin and depositional environment [23].

The ternary plot of regular steranes, expressed as C27%, C28%and C29%is used to compare between the de positional environment and source materials for the studied samples. The resource of C27 steranes is of marine origin, and that of C29 steranes is mainly from advanced plants, whereas C28 steranes consist of a mix of advanced plants and algae [15].

The samples extracted from Naokelekan and Barsarin formations are characterized by abundance of C27 over C28 and C29that was deposited exclusively under marine environment (Figures 12, 13).

Figure 12 Mass chromatograms for steranes, m/z 217, of extracted rock samples from Naokelekan and Barsarin formations of the studied wells
Figure 12

Mass chromatograms for steranes, m/z 217, of extracted rock samples from Naokelekan and Barsarin formations of the studied wells

Figure 13 Steranes ternary diagram of C27%, C28% and C29% concerning the selected extract samples using GC-MS m/z 217.
Figure 13

Steranes ternary diagram of C27%, C28% and C29% concerning the selected extract samples using GC-MS m/z 217.

5 Conclusion

Following conclusions have been drawn from the geochemical and molecular characterization studies of the Late Jurassic Naokelekan and Barsarin formations samples from Ma-1, At-1, and Sh-8 wells in the northwestern Iraq that,

  1. The OM in the Naokelekan Formation is mainly of Type II/III, whereas that of Barsarin Formation is dominantly, Type II.

  2. The TOC contents ranging from 0.52 to 6.07 wt% (1.7 wt%, av.) and 0.78 to 13.00 wt% (3.3 wt%, av.) for the Naokelekan and Barsarin formations, respectively, indicate that they have good source rock potential.

  3. The OM in the sediments of Naokelekan and Barsarin formations were deposited in an anoxic environment, as revealed by Pr/Ph, Pr/n-C17 and Ph/n-C18 ratios, and they also appear to be medium to low biodegraded.

  4. Carbon isotopic ratios of the saturate and aromatic fractions of the extracted samples from ternary plot of regular steranes of C27%, C28%and C29%, reveals that the OM in Naokelekan and Barsarin formations were derived mainly from the marine environment.

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Acknowledgement

The authors would like to thank StratoChem Laboratories, New Maadi, Cairo, Egypt for their technical support. Thanks are also extended to the Ministry of Natural Resources - Geological Survey in Erbil for providing cutting samples. Many thanks for Prof. Dr. Yawooz A. Kettanah, Duhok University, for revising the manuscript.

References

[1] Jassim S.Z., Goff J.C., Geology of Iraq. Published by Dolin, Prague and Moravian Museum, Brno, 2006Search in Google Scholar

[2] Aqrawi A.A.M., Goff J.C., Horbury A.D., Sadooni F.N., The petroleum geology of Iraq. Scientific Press Ltd, Beacon Field, UK, 2010Search in Google Scholar

[3] Al-Naqib S.O., Geology of Atrush area. MSc thesis, University of Mosul, Iraq, 1980Search in Google Scholar

[4] Al-Azzawi N.K., Hamdoon A.N., Structure and Geomorphology of Shaikhan Anticline-Northern Iraq. INJES, 2008, 8, 54-6310.33899/earth.2008.65696Search in Google Scholar

[5] Bellen R.C., Dunnington H.V., Wetzel R., Morton D., Lexique Stratigraphique Internal Asie, Iraq. International Geological Congress, Fasc. 10a, Paris: International Commission on Stratigraphy (in French), 1959Search in Google Scholar

[6] Abdula R.A., Balaky S.M., Nourmohamadi M.S., Piroui M., Microfacies analysis and depositional environment of the Sargelu Formation (Middle Jurassic) from Kurdistan Region, northern Iraq. Donn J. of Geol. Min. Res., 2015, 1, 1-26Search in Google Scholar

[7] Salae A.T.S., Stratigraphy and sedimentology of the Upper Jurassic succession Northern Iraq. MSc thesis, University of Baghdad, Iraq, 2001Search in Google Scholar

[8] Al-Ameri T.K., Al-Nagshbandi S.F., Age assessments and palynofacies of the Jurassic oil source rocks succession of North Iraq. Arab J. Giosci, 2015, 8, 759-77110.1007/s12517-013-1245-2Search in Google Scholar

[9] Abdula R.A., Stratigraphy and Lithology of Naokelekan Formation in Iraqi Kurdistan. IJES, 2016, 5, 7-17Search in Google Scholar

[10] Abdula R.A., Source Rock Assessment of Naokelekan Formation in Iraqi Kurdistan. JZS, 2017, 19, 103-12410.17656/jzs.10589Search in Google Scholar

[11] El Diasty W.S., El Beialy S.Y., Peters K.E., Batten D.J., Al-Beyati F.M., Mahdi A.Q., Haseeb, M.T., Organic geochemistry of the Middle-Upper Jurassic Naokelekan Formation in the Ajil and Balad oil fields, northern Iraq. JPSE, 2018, 350-362, DOI: 10.1016/j.petrol.2018.03.03110.1016/j.petrol.2018.03.031Search in Google Scholar

[12] Ditmar V., Team I.S., Geological conditions and hydrocarbon prospects of the Republic of Iraq, northern and central parts. Iraq NOC Report, 1971Search in Google Scholar

[13] Espitalie J., LaPorte J.L.,Madec M.,Marquis, F., LePlat P., Paulet J., Boutefeu A., Rapid method for source rock characterization and for determination of petroleum potentialand degree of evolution. Oil Gas Sci. Technol, 1977, 32, 23-4210.4043/2935-MSSearch in Google Scholar

[14] Peters K.E., Cassa M.R., Applied source rock geochemistry. In: Magoon L.B., Dow W.G (Eds), The petroleum system-from source to trap. AAPG, Memoir, 1994, 93-12010.1306/M60585C5Search in Google Scholar

[15] Peters K.E., Walters C.C., Moldowan J.M., The Biomarker guide, biomarkers and isotopes in petroleum exploration and earth history, Cambridge University Press, 200510.1017/CBO9781107326040Search in Google Scholar

[16] Espitalie J., Madec M., Tissot, B., Role of mineral matrix in kerogen pyrolysis: influence on petroleum generation and migration. AAPG Bulletin, 1980, 64, 59-6610.1016/0146-6380(84)90059-7Search in Google Scholar

[17] Espitalie J., Deroo G., Marquis F., Rock-Eval pyrolysis and its applications. Revue De L Institut Francais Du Petrole, 1985, 40, 563-57910.2516/ogst:1985035Search in Google Scholar

[18] Hunt J.M., Petroleumgeochemistry and geology, 2nd Edition. New York, W.H. Freeman, and Company, 1996Search in Google Scholar

[19] Moldowan J.M., Seifert W.K., Gallegos E.J., Relationship between petroleum composition and depositional environment of petroleum source rocks. AAPG Bulletin, 1985, 69, 1255-126810.1306/AD462BC8-16F7-11D7-8645000102C1865DSearch in Google Scholar

[20] Jarvie D.M., Tobey M.H., TOC, Rock-Eval and SR Analyzer Interpretive Guidelines. In Application Note 99-4. Humble Instruments and Services, In: Geochemical services Division Texas, 1999Search in Google Scholar

[21] Abdula R.A., Organic geochemical assessment of Jurassic potential source rock from Zab-1 well, Iraqi Kurdistan, IBGM, 2016, 12, 53-64Search in Google Scholar

[22] Ten Haven H.L., De Leeuw J.W., Rullkötter J., Damste J.S., Restricted utility of the pristane/phytane ratio as a palaeoenvironmental indicator. Nature 330, 1987, 641-64310.1038/330641a0Search in Google Scholar

[23] Jalees M.I., Tahira F., Saleem H., Study on the geochemical correlation of crude oils of Paleocene and Jurassic ages from the Potowar Indus Basin in northern Pakistan. Chinese J. of Geochem., 2010, 29, 82-9310.1007/s11631-010-0082-1Search in Google Scholar

[24] Tissot B.P., Welte D.H., Petroleum formation and occurrence, second ed. Springer -Verlag, Berlin, 198410.1007/978-3-642-87813-8Search in Google Scholar

[25] Mohialdeen I.M.J.,Mustafa K.A., Salih D.A., Sephton M.A., Saeed D.A., Biomarker analysis of the upper Jurassic Naokelekan and Barsarin formations in the Miran Well-2, Miran oil field, Kurdistan Region, Iraq. Arab J. Giosci., 2018, 11, DOI: 10.1007/s12517-018-3405-x10.1007/s12517-018-3405-xSearch in Google Scholar

[26] Osuji L.C., Antia B.C., Geochemical implication of some chemical fossils as indicators of petroleum source rocks. J. Appl. Sci. Environ. Mgt., 2005, 9, 45-49Search in Google Scholar

[27] Obermajer M., Fowler M.G., Snowdon L.R., Depositional environment and oil generation in Ordovician source rocks from southwestern Ontario, Canada. Organic geochemical and petrological approach. AAPG Bulletin,1999, 83, 1426-145310.1306/E4FD41D9-1732-11D7-8645000102C1865DSearch in Google Scholar

[28] Sofer Z., Stable carbon isotope compositions of crude oils: application to source depositional environments and petroleum alteration. AAPG Bulletin, 1984, 68, 31-4910.1306/AD460963-16F7-11D7-8645000102C1865DSearch in Google Scholar

[29] Demaison G., Huizinga B.J., Genetic classification of petroleum systems (1). AAPG Bulletin, 1991, 75,1626-16410.1306/0C9B29BB-1710-11D7-8645000102C1865DSearch in Google Scholar

Received: 2018-09-10
Accepted: 2019-02-16
Published Online: 2019-12-18

© 2019 S. J. Al-Atroshi et al., published by De Gruyter

This work is licensed under the Creative Commons Attribution 4.0 Public License.

Articles in the same Issue

  1. Regular Articles
  2. 2D Seismic Interpretation of the Meyal Area, Northern Potwar Deform Zone, Potwar Basin, Pakistan
  3. A new method of lithologic identification and distribution characteristics of fine - grained sediments: A case study in southwest of Ordos Basin, China
  4. Modified Gompertz sigmoidal model removing fine-ending of grain-size distribution
  5. Diagenesis and its influence on reservoir quality and oil-water relative permeability: A case study in the Yanchang Formation Chang 8 tight sandstone oil reservoir, Ordos Basin, China
  6. Evaluation of AHRS algorithms for Foot-Mounted Inertial-based Indoor Navigation Systems
  7. Identification and evaluation of land use vulnerability in a coal mining area under the coupled human-environment
  8. Hydrocarbon Generation Potential of Chia Gara Formation in Three Selected Wells, Northern Iraq
  9. Source Analysis of Silicon and Uranium in uranium-rich shale in the Xiuwu Basin, Southern China
  10. Lithologic heterogeneity of lacustrine shale and its geological significance for shale hydrocarbon-a case study of Zhangjiatan Shale
  11. Characterization of soil permeability in the former Lake Texcoco, Mexico
  12. Detrital zircon trace elements from the Mesozoic Jiyuan Basin, central China and its implication on tectonic transition of the Qinling Orogenic Belt
  13. Turkey OpenStreetMap Dataset - Spatial Analysis of Development and Growth Proxies
  14. Morphological Changes of the Lower Ping and Chao Phraya Rivers, North and Central Thailand: Flood and Coastal Equilibrium Analyses
  15. Landscape Transformations in Rapidly Developing Peri-urban Areas of Accra, Ghana: Results of 30 years
  16. Division of shale sequences and prediction of the favorable shale gas intervals: an example of the Lower Cambrian of Yangtze Region in Xiuwu Basin
  17. Fractal characteristics of nanopores in lacustrine shales of the Triassic Yanchang Formation, Ordos Basin, NW China
  18. Selected components of geological structures and numerical modelling of slope stability
  19. Spatial data quality and uncertainty publication patterns and trends by bibliometric analysis
  20. Application of microstructure classification for the assessment of the variability of geological-engineering and pore space properties in clay soils
  21. Shear failure modes and AE characteristics of sandstone and marble fractures
  22. Ice Age theory: a correspondence between Milutin Milanković and Vojislav Mišković
  23. Are Serbian tourists worried? The effect of psychological factors on tourists’ behavior based on the perceived risk
  24. Real-Time Map Matching: A New Algorithm Integrating Spatio-Temporal Proximity and Improved Weighted Circle
  25. Characteristics and hysteresis of saturated-unsaturated seepage of soil landslides in the Three Gorges Reservoir Area, China
  26. Petrographical and geophysical investigation of the Ecca Group between Fort Beaufort and Grahamstown, in the Eastern Cape Province, South Africa
  27. Ecological risk assessment of geohazards in Natural World Heritage Sites: an empirical analysis of Bogda, Tianshan
  28. Integrated Subsurface Temperature Modeling beneath Mt. Lawu and Mt. Muriah in The Northeast Java Basin, Indonesia
  29. Go social for your own safety! Review of social networks use on natural disasters – case studies from worldwide
  30. Forestry Aridity Index in Vojvodina, North Serbia
  31. Natural Disasters vs Hotel Industry Resilience: An Exploratory Study among Hotel Managers from Europe
  32. Using Monarch Butterfly Optimization to Solve the Emergency Vehicle Routing Problem with Relief Materials in Sudden Disasters
  33. Potential influence of meteorological variables on forest fire risk in Serbia during the period 2000-2017
  34. Controlling factors on the geochemistry of Al-Shuaiba and Al-Mejarma coastal lagoons, Red Sea, Saudi Arabia
  35. The Influence of Kaolinite - Illite toward mechanical properties of Claystone
  36. Two critical books in the history of loess investigation: ‘Charakteristik der Felsarten’ by Karl Caesar von Leonhard and ‘Principles of Geology’ by Charles Lyell
  37. The Mechanism and Control Technology of Strong Strata Behavior in Extra-Thick Coal Seam Mining Influenced by Overlying Coal Pillar
  38. Shared Aerial Drone Videos — Prospects and Problems for Volunteered Geographic Information Research
  39. Stable isotopes of C and H in methane fermentation of agriculture substrates at different temperature conditions
  40. Prediction of Compression and Swelling Index Parameters of Quaternary Sediments from Index Tests at Mersin District
  41. Detection of old scattered windthrow using low cost resources. The case of Storm Xynthia in the Vosges Mountains, 28 February 2010
  42. Remediation of Copper and Zinc from wastewater by modified clay in Asir region southwest of Saudi Arabia
  43. Sedimentary facies of Paleogene lacustrine dolomicrite and implications for petroleum reservoirs in the southern Qianjiang Depression, China
  44. Correlation between ore particle flow pattern and velocity field through multiple drawpoints under the influence of a flexible barrier
  45. Atmospheric refractivity estimation from AIS signal power using the quantum-behaved particle swarm optimization algorithm
  46. A geophysical and hydro physico-chemical study of the contaminant impact of a solid waste landfill (swl) in King Williams’ Town, Eastern Cape, South Africa
  47. Landscape characterization using photographs from crowdsourced platforms: content analysis of social media photographs
  48. A Study on Transient Electromagnetic Interpretation Method Based on the Seismic Wave Impedance Inversion Model
  49. Stratigraphy of Architectural Elements of a Buried Monogenetic Volcanic System
  50. Variable secondary porosity modeling of carbonate rocks based on μ-CT images
  51. Traditional versus modern settlement on torrential alluvial fans considering the danger of debris flows: a case study of the Upper Sava Valley (NW Slovenia)
  52. The Influence of Gangue Particle size and Gangue Feeding Rate on Safety and Service Life of the Suspended Buffer’s Spring
  53. Research on the Transition Section Length of the Mixed Workface Using Gangue Backfilling Method and Caving Method
  54. Rainfall erosivity and extreme precipitation in the Pannonian basin
  55. Structure of the Sediment and Crust in the Northeast North China Craton from Improved Sequential H-k Stacking Method
  56. Planning Activities Improvements Responding Local Interests Change through Participatory Approach
  57. GIS-based landslide susceptibility mapping using bivariate statistical methods in North-western Tunisia
  58. Uncertainty based multi-step seismic analysis for near-surface imaging
  59. Deformation monitoring and prediction for residential areas in the Panji mining area based on an InSAR time series analysis and the GM-SVR model
  60. Statistical and expert-based landslide susceptibility modeling on a national scale applied to North Macedonia
  61. Natural hazards and their impact on rural settlements in NE Romania – A cartographical approach
  62. Rock fracture initiation and propagation by mechanical and hydraulic impact
  63. Influence of Rapid Transit on Accessibility Pattern and Economic Linkage at Urban Agglomeration Scale in China
  64. Near Infrared Spectroscopic Study of Trioctahedral Chlorites and Its Remote Sensing Application
  65. Problems with collapsible soils: Particle types and inter-particle bonding
  66. Unification of data from various seismic catalogues to study seismic activity in the Carpathians Mountain arc
  67. Quality assessment of DEM derived from topographic maps for geomorphometric purposes
  68. Remote Sensing Monitoring of Soil Moisture in the Daliuta Coal Mine Based on SPOT 5/6 and Worldview-2
  69. Utilizing Maximum Entropy Spectral Analysis (MESA) to identify Milankovitch cycles in Lower Member of Miocene Zhujiang Formation in north slope of Baiyun Sag, Pearl River Mouth Basin, South China Sea
  70. Stability Analysis of a Slurry Trench in Cohesive-Frictional Soils
  71. Integrating Landsat 7 and 8 data to improve basalt formation classification: A case study at Buon Ma Thuot region, Central Highland, Vietnam
  72. Assessment of the hydrocarbon potentiality of the Late Jurassic formations of NW Iraq: A case study based on TOC and Rock-Eval pyrolysis in selected oil-wells
  73. Rare earth element geochemistry of sediments from the southern Okinawa Trough since 3 ka: Implications for river-sea processes and sediment source
  74. Effect of gas adsorption-induced pore radius and effective stress on shale gas permeability in slip flow: New Insights
  75. Development of the Narva-Jõesuu beach, mineral composition of beach deposits and destruction of the pier, southeastern coast of the Gulf of Finland
  76. Selecting fracturing interval for the exploitation of tight oil reservoirs from logs: a case study
  77. A comprehensive scheme for lithological mapping using Sentinel-2A and ASTER GDEM in weathered and vegetated coastal zone, Southern China
  78. Sedimentary model of K-Successions Sandstones in H21 Area of Huizhou Depression, Pearl River Mouth Basin, South China Sea
  79. A non-uniform dip slip formula to calculate the coseismic deformation: Case study of Tohoku Mw9.0 Earthquake
  80. Decision trees in environmental justice research — a case study on the floods of 2001 and 2010 in Hungary
  81. The Impacts of Climate Change on Maximum Daily Discharge in the Payab Jamash Watershed, Iran
  82. Mass tourism in protected areas – underestimated threat? Polish National Parks case study
  83. Decadal variations of total organic carbon production in the inner-shelf of the South China Sea and East China Sea
  84. Hydrogeothermal potentials of Rogozna mountain and possibility of their valorization
  85. Postglacial talus slope development imaged by the ERT method: comparison of slopes from SW Spitsbergen, Norway and Tatra Mountains, Poland
  86. Seismotectonics of Malatya Fault, Eastern Turkey
  87. Investigating of soil features and landslide risk in Western-Atakent (İstanbul) using resistivity, MASW, Microtremor and boreholes methods
  88. Assessment of Aquifer Vulnerability Using Integrated Geophysical Approach in Weathered Terrains of South China
  89. An integrated analysis of mineralogical and microstructural characteristics and petrophysical properties of carbonate rocks in the lower Indus Basin, Pakistan
  90. Applicability of Hydrological Models for Flash Flood Simulation in Small Catchments of Hilly Area in China
  91. Heterogeneity analysis of shale reservoir based on multi-stage pumping data
https://doi.org/10.1515/geo-2019-0071
Keywords for this article
Naokelekan Fm.; Barsarin Fm.; Mangesh; Atrush; Shaikhan; Rock-Eval; Biomarker
Creative Commons
BY 4.0

Articles in the same Issue

  1. Regular Articles
  2. 2D Seismic Interpretation of the Meyal Area, Northern Potwar Deform Zone, Potwar Basin, Pakistan
  3. A new method of lithologic identification and distribution characteristics of fine - grained sediments: A case study in southwest of Ordos Basin, China
  4. Modified Gompertz sigmoidal model removing fine-ending of grain-size distribution
  5. Diagenesis and its influence on reservoir quality and oil-water relative permeability: A case study in the Yanchang Formation Chang 8 tight sandstone oil reservoir, Ordos Basin, China
  6. Evaluation of AHRS algorithms for Foot-Mounted Inertial-based Indoor Navigation Systems
  7. Identification and evaluation of land use vulnerability in a coal mining area under the coupled human-environment
  8. Hydrocarbon Generation Potential of Chia Gara Formation in Three Selected Wells, Northern Iraq
  9. Source Analysis of Silicon and Uranium in uranium-rich shale in the Xiuwu Basin, Southern China
  10. Lithologic heterogeneity of lacustrine shale and its geological significance for shale hydrocarbon-a case study of Zhangjiatan Shale
  11. Characterization of soil permeability in the former Lake Texcoco, Mexico
  12. Detrital zircon trace elements from the Mesozoic Jiyuan Basin, central China and its implication on tectonic transition of the Qinling Orogenic Belt
  13. Turkey OpenStreetMap Dataset - Spatial Analysis of Development and Growth Proxies
  14. Morphological Changes of the Lower Ping and Chao Phraya Rivers, North and Central Thailand: Flood and Coastal Equilibrium Analyses
  15. Landscape Transformations in Rapidly Developing Peri-urban Areas of Accra, Ghana: Results of 30 years
  16. Division of shale sequences and prediction of the favorable shale gas intervals: an example of the Lower Cambrian of Yangtze Region in Xiuwu Basin
  17. Fractal characteristics of nanopores in lacustrine shales of the Triassic Yanchang Formation, Ordos Basin, NW China
  18. Selected components of geological structures and numerical modelling of slope stability
  19. Spatial data quality and uncertainty publication patterns and trends by bibliometric analysis
  20. Application of microstructure classification for the assessment of the variability of geological-engineering and pore space properties in clay soils
  21. Shear failure modes and AE characteristics of sandstone and marble fractures
  22. Ice Age theory: a correspondence between Milutin Milanković and Vojislav Mišković
  23. Are Serbian tourists worried? The effect of psychological factors on tourists’ behavior based on the perceived risk
  24. Real-Time Map Matching: A New Algorithm Integrating Spatio-Temporal Proximity and Improved Weighted Circle
  25. Characteristics and hysteresis of saturated-unsaturated seepage of soil landslides in the Three Gorges Reservoir Area, China
  26. Petrographical and geophysical investigation of the Ecca Group between Fort Beaufort and Grahamstown, in the Eastern Cape Province, South Africa
  27. Ecological risk assessment of geohazards in Natural World Heritage Sites: an empirical analysis of Bogda, Tianshan
  28. Integrated Subsurface Temperature Modeling beneath Mt. Lawu and Mt. Muriah in The Northeast Java Basin, Indonesia
  29. Go social for your own safety! Review of social networks use on natural disasters – case studies from worldwide
  30. Forestry Aridity Index in Vojvodina, North Serbia
  31. Natural Disasters vs Hotel Industry Resilience: An Exploratory Study among Hotel Managers from Europe
  32. Using Monarch Butterfly Optimization to Solve the Emergency Vehicle Routing Problem with Relief Materials in Sudden Disasters
  33. Potential influence of meteorological variables on forest fire risk in Serbia during the period 2000-2017
  34. Controlling factors on the geochemistry of Al-Shuaiba and Al-Mejarma coastal lagoons, Red Sea, Saudi Arabia
  35. The Influence of Kaolinite - Illite toward mechanical properties of Claystone
  36. Two critical books in the history of loess investigation: ‘Charakteristik der Felsarten’ by Karl Caesar von Leonhard and ‘Principles of Geology’ by Charles Lyell
  37. The Mechanism and Control Technology of Strong Strata Behavior in Extra-Thick Coal Seam Mining Influenced by Overlying Coal Pillar
  38. Shared Aerial Drone Videos — Prospects and Problems for Volunteered Geographic Information Research
  39. Stable isotopes of C and H in methane fermentation of agriculture substrates at different temperature conditions
  40. Prediction of Compression and Swelling Index Parameters of Quaternary Sediments from Index Tests at Mersin District
  41. Detection of old scattered windthrow using low cost resources. The case of Storm Xynthia in the Vosges Mountains, 28 February 2010
  42. Remediation of Copper and Zinc from wastewater by modified clay in Asir region southwest of Saudi Arabia
  43. Sedimentary facies of Paleogene lacustrine dolomicrite and implications for petroleum reservoirs in the southern Qianjiang Depression, China
  44. Correlation between ore particle flow pattern and velocity field through multiple drawpoints under the influence of a flexible barrier
  45. Atmospheric refractivity estimation from AIS signal power using the quantum-behaved particle swarm optimization algorithm
  46. A geophysical and hydro physico-chemical study of the contaminant impact of a solid waste landfill (swl) in King Williams’ Town, Eastern Cape, South Africa
  47. Landscape characterization using photographs from crowdsourced platforms: content analysis of social media photographs
  48. A Study on Transient Electromagnetic Interpretation Method Based on the Seismic Wave Impedance Inversion Model
  49. Stratigraphy of Architectural Elements of a Buried Monogenetic Volcanic System
  50. Variable secondary porosity modeling of carbonate rocks based on μ-CT images
  51. Traditional versus modern settlement on torrential alluvial fans considering the danger of debris flows: a case study of the Upper Sava Valley (NW Slovenia)
  52. The Influence of Gangue Particle size and Gangue Feeding Rate on Safety and Service Life of the Suspended Buffer’s Spring
  53. Research on the Transition Section Length of the Mixed Workface Using Gangue Backfilling Method and Caving Method
  54. Rainfall erosivity and extreme precipitation in the Pannonian basin
  55. Structure of the Sediment and Crust in the Northeast North China Craton from Improved Sequential H-k Stacking Method
  56. Planning Activities Improvements Responding Local Interests Change through Participatory Approach
  57. GIS-based landslide susceptibility mapping using bivariate statistical methods in North-western Tunisia
  58. Uncertainty based multi-step seismic analysis for near-surface imaging
  59. Deformation monitoring and prediction for residential areas in the Panji mining area based on an InSAR time series analysis and the GM-SVR model
  60. Statistical and expert-based landslide susceptibility modeling on a national scale applied to North Macedonia
  61. Natural hazards and their impact on rural settlements in NE Romania – A cartographical approach
  62. Rock fracture initiation and propagation by mechanical and hydraulic impact
  63. Influence of Rapid Transit on Accessibility Pattern and Economic Linkage at Urban Agglomeration Scale in China
  64. Near Infrared Spectroscopic Study of Trioctahedral Chlorites and Its Remote Sensing Application
  65. Problems with collapsible soils: Particle types and inter-particle bonding
  66. Unification of data from various seismic catalogues to study seismic activity in the Carpathians Mountain arc
  67. Quality assessment of DEM derived from topographic maps for geomorphometric purposes
  68. Remote Sensing Monitoring of Soil Moisture in the Daliuta Coal Mine Based on SPOT 5/6 and Worldview-2
  69. Utilizing Maximum Entropy Spectral Analysis (MESA) to identify Milankovitch cycles in Lower Member of Miocene Zhujiang Formation in north slope of Baiyun Sag, Pearl River Mouth Basin, South China Sea
  70. Stability Analysis of a Slurry Trench in Cohesive-Frictional Soils
  71. Integrating Landsat 7 and 8 data to improve basalt formation classification: A case study at Buon Ma Thuot region, Central Highland, Vietnam
  72. Assessment of the hydrocarbon potentiality of the Late Jurassic formations of NW Iraq: A case study based on TOC and Rock-Eval pyrolysis in selected oil-wells
  73. Rare earth element geochemistry of sediments from the southern Okinawa Trough since 3 ka: Implications for river-sea processes and sediment source
  74. Effect of gas adsorption-induced pore radius and effective stress on shale gas permeability in slip flow: New Insights
  75. Development of the Narva-Jõesuu beach, mineral composition of beach deposits and destruction of the pier, southeastern coast of the Gulf of Finland
  76. Selecting fracturing interval for the exploitation of tight oil reservoirs from logs: a case study
  77. A comprehensive scheme for lithological mapping using Sentinel-2A and ASTER GDEM in weathered and vegetated coastal zone, Southern China
  78. Sedimentary model of K-Successions Sandstones in H21 Area of Huizhou Depression, Pearl River Mouth Basin, South China Sea
  79. A non-uniform dip slip formula to calculate the coseismic deformation: Case study of Tohoku Mw9.0 Earthquake
  80. Decision trees in environmental justice research — a case study on the floods of 2001 and 2010 in Hungary
  81. The Impacts of Climate Change on Maximum Daily Discharge in the Payab Jamash Watershed, Iran
  82. Mass tourism in protected areas – underestimated threat? Polish National Parks case study
  83. Decadal variations of total organic carbon production in the inner-shelf of the South China Sea and East China Sea
  84. Hydrogeothermal potentials of Rogozna mountain and possibility of their valorization
  85. Postglacial talus slope development imaged by the ERT method: comparison of slopes from SW Spitsbergen, Norway and Tatra Mountains, Poland
  86. Seismotectonics of Malatya Fault, Eastern Turkey
  87. Investigating of soil features and landslide risk in Western-Atakent (İstanbul) using resistivity, MASW, Microtremor and boreholes methods
  88. Assessment of Aquifer Vulnerability Using Integrated Geophysical Approach in Weathered Terrains of South China
  89. An integrated analysis of mineralogical and microstructural characteristics and petrophysical properties of carbonate rocks in the lower Indus Basin, Pakistan
  90. Applicability of Hydrological Models for Flash Flood Simulation in Small Catchments of Hilly Area in China
  91. Heterogeneity analysis of shale reservoir based on multi-stage pumping data
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