A Review on Greensand Reservoirs’ Petrophysical Controls

Abstract

This review provides a comprehensive analysis of the petrophysical controls influencing greensand reservoirs, with an emphasis on the role of glauconite and associated clay minerals in determining porosity, permeability, and water saturation. Greensands contain iron-rich clay minerals that exert paramagnetic and conductive effects, challenging conventional well-log interpretations and often leading to biased estimates of reservoir parameters. Several challenges for petrophysical property measurements are faced in the laboratory due to clay-induced pore-throat obstruction and microporosity, which underscores the importance of tailored interpretation workflows and data integration. In this paper we highlight the necessity of integrated approaches such as combining core analysis, spectral gamma-ray, and nuclear magnetic resonance (NMR) logging with conventional well logs to calibrate petrophysical models using shale–sand water saturation models, such as Waxman–Smits and Simandoux, to better characterise economical pay zones. Finally, future research directions are indicated, which include refining the calibration of saturation and permeability models, advancing rock-typing methodologies, and understanding mineralogical influences on reservoir quality to optimise hydrocarbon recovery from greensand reservoirs.

1. Introduction

Greensand reservoirs are present in mature basins and marginal plays, where reliable petrophysical evaluation is essential to reduce uncertainty in reserve calculations and optimising production planning. Greensands—or glauconitic sandstones—are a complex rock type that produce oil or gas throughout the world, including the North Sea region of northern Europe, New Zealand, India, Brazil, Argentina, and Chile (see Table 1). These siliciclastic rocks are distinguished due to the predominant presence of glauconite along with other clay minerals such as illite–smectite mixed layers and chlorite in minor proportions. Often greensands have poor to moderate porosity (<15% v/v) and ultra-low to low permeability, classifying them as tight reservoirs, making hydraulic fracturing the only viable technology to make them economically producible.

In addition to their relevance as hydrocarbon-bearing formations, greensands are of increasing interest within the mineralogical community due to their high content of the clay mineral glauconite. The petrophysical behavior of these reservoirs is fundamentally governed by the mineralogical composition, diagenetic evolution, and microstructural characteristics of glauconite and associated clays. These minerals influence key reservoir properties, including porosity, permeability, and water saturation, through their surface area, cation-exchange capacity, and microporosity. This review aligns with the scope of minerals by highlighting the mineralogical controls on reservoir quality and by emphasising the role of clay minerals in subsurface energy systems, including their implications for hydrocarbon production, CO₂ storage, and even agricultural applications.

The term “greensand” stems from the greenish colour of the rock, which is primarily attributed to the presence of glauconite but is also enhanced by other clay minerals such as chlorite and illite–smectite [1,2,3,4,5]. The presence of these clay minerals in greensands results in several unique properties, such as a bimodal pore-size distribution due to the presence of macropores between framework grains and micropores between clay minerals [1]. Chemical analysis suggests that they often have a high iron, potassium [6], and boron content [7]. They also have a moderate cation-exchange capacity (7.8 to 32.4 MEQ/100 g) [8] due to the high specific surface area owing to the presence of mixed clay minerals. These features significantly affect commonly used wire-line log measurements (e.g., gamma-ray, density, neutron, and resistivity measurements), making standard well-log interpretation techniques unreliable for estimating porosity, clay volume, and water saturation.

Archie’s [9] standard water saturation equation remains widely used to estimate hydrocarbon volumes in clay-bearing sandstones, despite being formulated for clean sandstones without conductive clay minerals. In reservoirs like greensands, the assumptions behind Archie’s model break down, particularly in conditions of low water salinity or in rocks with high clay content (e.g., [10]). This challenge is part of the “shaly sand problem,” where clay minerals distort resistivity-based saturation estimates. Glauconite, in particular, complicates interpretation due to its dual porosity and elevated iron content, which significantly increases rock conductivity. These properties result in low resistivity readings and misleading water saturation estimates. While shale–sand water saturation models such as the Waxman–Smits [11] and the dual-water models [12] attempt to incorporate the effects of clay conductivity, their application is still limited, and their parameters are not well calibrated for glauconitic systems. The selection of a suitable water saturation model for greensand reservoirs is still debated, especially when logs are acquired in low-salinity environments or reservoirs with mixed clay mineralogy.

Net pay is one of the most valuable outcomes of petrophysical interpretation and evaluation; however, greensand reservoirs are inherently complex. Due to their heterogeneous mineralogy, laboratory services confront issues in routine core analysis (RCA) programs, delaying petrophysical and petrological measurements; hence, in many fields, interpreters rely heavily on logging tools. In addition, the cut-off criteria for porosity, clay volume, and water saturation are often inconsistent, and applying fixed thresholds often leads to poor reservoir characterisation. Advanced tools like nuclear magnetic resonance (NMR) and mercury injection capillary pressure (MICP) have improved estimates of fluid saturation and permeability by probing pore structure more directly [13]. These methods also enable cross-calibration (e.g., using NMR T₂ distributions to infer pore-body sizes and MICP to define pore throats), but their integration into consistent workflows tailored to greensands remains underdeveloped.

A few published studies have proposed petrophysical models and workflows for greensand reservoirs (e.g., [8,14,15,16,17,18,19]); however, these are case-specific and do not fully address the underlying physical mechanisms controlling petrophysical behaviour in greensands. However, a systematic literature review on glauconite research undertaken by Nong et al. [20] indicates that research prospects are increasing, with a special focus on fertilisation, composition features, and provenance as emerging frontiers. This trend is further supported by recent advances in glauconite applications in agriculture, as reviewed by Dasi et al. [21], highlighting the mineral’s broader relevance beyond subsurface energy systems.

This review paper critically examines the petrophysical properties of greensand reservoirs, focusing on

• Key physical and mineralogical controls on porosity, permeability, and irreducible water saturation;
• Measurement and interpretation challenges, particularly in log analysis and saturation modelling;
• Recent advances in core–log integration and workflow development for more reliable reservoir characterisation.

By synthesising the available literature in English and Spanish and identifying the limitations of current models and assumptions, this review contributes to the development of more appropriate interpretation frameworks. It emphasises that many conventional petrophysical tools and models—particularly those based on clean sandstones—are inadequate for glauconitic systems. The review concludes with recommendations for integrated interpretation workflows that combine advanced logging methods, core and laboratory calibration, and tailored petrophysical models—incorporating mineralogical complexity, adjusted NMR parameters, and electrochemical analysis—while emphasising the need for future research in core–log–digital rock physics integration and machine learning approaches to improve reservoir characterisation and management in greensand reservoirs.

Table 1. Porosity and permeability data reported from some greensand reservoirs worldwide.

Reservoir Type	Reservoir Name	Location	Geological Period or Epoch	Porosity * (%v/v)	Permeability * (mD)	Glauconite Content * (%v/v)	Ref.
Oil	Matulla Formation from Nezzazat Group	Lower Senonian, Gulf of Suez, Egypt	Upper Cretaceous	3.5 to 25	<1 to 90	20 to 45	[8]
Oil and gas	Glauconite member from Mannville Group	Lake Newell, Southern Alberta, Canada	Lower Cretaceous	9 to 33	10 to 10,200	Not available	[22]
Tight oil	Albian “A” Sand Formation from Greensand Group	North Celtic Sea Basin	Lower Cretaceous	≤30	≤50	≤45	[23]
Oil	Pona Reservoir, Chonta Formation	Peruvian forest region	Cretaceous	1 to 20	1 to 1000	Not available	[24]
Tight oil	Caballos Formation	Putumayo Basin, Colombia	Lower Cretaceous	2 to 19	0.01 to 1200	10 to 60	[25]
Tight oil	Mardie Greensand Formation	Carnarvon Basin, Australia	Early Cretaceous	15 to 28	0 to 100	Not available	[14,15]
Oil	Hermod and Ty Formations	Siri Canyon, Danish North Sea	Palaeocene	25 to 40	60 to 1000	20 to 30	[26]
Tight gas	Magallanes Formation	Campo Indio field, Austral Basin, Argentina	Upper Cretaceous	15 to 35	0.01 to 1	Not able to be determined **	[9,10]
Tight gas	Zona Glauconitica	Austral-Magallanes Basin, Chile	Palaeocene	10 to 25	0.001 to 1	Not able to be determined **	[18]
Tight oil	Upper T of Napo Formation	Oriente Basin, Ecuador	Cretaceous	5 to 20	≤500	10 to 40	[27]

* Reported either from core analysis or reservoir evaluation. ** XRD analysis could not identify glauconite since it overlapped with illite presence.

Table 1. Porosity and permeability data reported from some greensand reservoirs worldwide.

Reservoir Type	Reservoir Name	Location	Geological Period or Epoch	Porosity * (%v/v)	Permeability * (mD)	Glauconite Content * (%v/v)	Ref.
Oil	Matulla Formation from Nezzazat Group	Lower Senonian, Gulf of Suez, Egypt	Upper Cretaceous	3.5 to 25	<1 to 90	20 to 45	[8]
Oil and gas	Glauconite member from Mannville Group	Lake Newell, Southern Alberta, Canada	Lower Cretaceous	9 to 33	10 to 10,200	Not available	[22]
Tight oil	Albian “A” Sand Formation from Greensand Group	North Celtic Sea Basin	Lower Cretaceous	≤30	≤50	≤45	[23]
Oil	Pona Reservoir, Chonta Formation	Peruvian forest region	Cretaceous	1 to 20	1 to 1000	Not available	[24]
Tight oil	Caballos Formation	Putumayo Basin, Colombia	Lower Cretaceous	2 to 19	0.01 to 1200	10 to 60	[25]
Tight oil	Mardie Greensand Formation	Carnarvon Basin, Australia	Early Cretaceous	15 to 28	0 to 100	Not available	[14,15]
Oil	Hermod and Ty Formations	Siri Canyon, Danish North Sea	Palaeocene	25 to 40	60 to 1000	20 to 30	[26]
Tight gas	Magallanes Formation	Campo Indio field, Austral Basin, Argentina	Upper Cretaceous	15 to 35	0.01 to 1	Not able to be determined **	[9,10]
Tight gas	Zona Glauconitica	Austral-Magallanes Basin, Chile	Palaeocene	10 to 25	0.001 to 1	Not able to be determined **	[18]
Tight oil	Upper T of Napo Formation	Oriente Basin, Ecuador	Cretaceous	5 to 20	≤500	10 to 40	[27]

* Reported either from core analysis or reservoir evaluation. ** XRD analysis could not identify glauconite since it overlapped with illite presence.

2. Geological and Mineral Framework of Greensands

2.1. Mineral Composition and Diagenesis

This subsection outlines the primary mineral constituents and the process of glauconitisation that governs greensand reservoirs, with an emphasis on how mineral evolution influences petrophysical behaviour.

Greensands are iron-rich sandstones dominated by the clay mineral glauconite, a member of the mica group. Other clay minerals such as chlorite, smectite, and illite are frequently present [1,2,3,4,5]. Glauconitic pellets form through a process called glauconitisation, in which K-poor smectite transforms into K-rich glauconite mica pellets during burial diagenesis [6].

As glauconitisation advances, potassium and iron contents increase within these pellets, while aluminium content decreases (Figure 1). The resulting sedimentary rock comprises a complex mixture of clay minerals, with diagenetic alterations that directly affect the texture and reservoir quality of greensands [6]. For example, transformations from smectite to illite or glauconite alter the cation-exchange capacity and permeability. The development of clay mineral coatings or pore-filling cements during diagenesis modifies both the intergranular cohesion and the pore-throat geometry, significantly affecting porosity and increasing surface area. Other clay minerals—chlorite, smectite, and illite—also play significant roles in the mineralogical and petrophysical behaviour of greensands. Chlorite generally occurs as a pore-filling and grain-coating material, whereas smectite and illite commonly exist as fine matrix minerals or mixed-layer clays (see, e.g., [1,2]). As shown in Figure 2, these minerals often act as grain coating or pore-filling phases, contributing to microporosity and reduced permeability.

Figure 1. Glauconitisation model in the studied grains (modified after López-Quirós et al. [28], following the concepts of Odin and Matter [29] and Baldermann et al. [30]). Adapted from López-Quirós et al. [31]. Nascent stage: After deposition at the seafloor, glauconite grains begin forming within semi-confined environments. Early pore networks start developing alongside the incorporation of detrital clay minerals. During this stage, dissolution of carbonate components occurs, and iron is primarily present as Fe³⁺-smectite precursors. Microbial oxidation of organic matter contributes to the early geochemical conditions, typically over a period of ~10–10³ years. Slightly evolved stage: The grains mature as ions from the formation water re-accommodated within the mineral structure, promoting the neoformation of glauconitic smectite (G/S). Detrital minerals gradually diminish, coinciding with an increase in Fe and K ion content and the transformation of iron oxides to Fe²⁺ and Fe³⁺ forms. This stage generally spans ~10³–10⁴ years. Evolved stage: Continued recrystallisation and rearrangement of mineral composition result in more consolidated grains with the development of superficial cracks. Crystal growth accelerates particularly in the centre of the grain. The chemical composition evolves significantly as Si, Al in octahedral coordination (Al^VI), Mg, Ca, and Na are progressively substituted by Al in tetrahedral coordination (Al^IV), Fe (primarily Fe²⁺), and K. This reaction from Fe(III)–smectite to glauconite occurs over a period of between ~10⁴ and 10⁶ years. Highly evolved stage: At this final stage, a new generation of glauconitic minerals forms on the grain periphery, encapsulating the original glaucony pellets. This process involves advanced recrystallisation, leading to the development of glauconitic micas with distinctive microtextures, such as authigenic flakes and rosettes, indicative of full maturation.

Figure 2. Diagram of greensand major grains and clay distribution types as grain-coating and -filling pore throats; glauconite exhibits microporosity [32].

2.2. Diagenetic Alteration and Textural Controls

Beyond mineral composition, the diagenetic evolution of greensands plays a critical role in shaping reservoir quality. This subsection examines grain morphology, cementation, and depositional textures that influence pore structure and connectivity.

Glauconite grains exhibit diverse morphologies, including spherical, ovoid, tabular, vermiform, and lobate shapes, and may be incorporated within microfossils [33]. These grains typically tend to be part of the rock framework rather than acting as a pore-filling phase, thereby reducing the pore-throat area and connectivity. Silica cement is typically present in glauconitic sandstones that strengthen the pore network but reduce the overall porosity. Carbonate (e.g., calcite) or berthierine cement may also occur locally, blocking intergranular pore throats. Some authors describe the glauconitic grains as having angular to subangular (i.e., irregular) shapes with highly rough surfaces. Sorting varies from locally poor to moderate, while packing ranges from moderately poor to a tight arrangement (e.g., [27,34,35,36]). Therefore, reservoir quality in greensands is principally controlled by their characteristic poor sorting, rough grain surfaces, and tight grain packing—features inherited from depositional conditions and modified by diagenesis. These textural heterogeneities lead to complex pore networks with restricted pore-throat sizes and reduced connectivity, especially where clay minerals are abundant.

These textural features are not only the result of diagenesis processes but are also inherited from the original depositional environment. As shown in Figure 1, greensand formation is closely tied to specific depositional environments, typically low-energy settings with slow sedimentation rates, such as outer shelf or upper slope conditions. These environments favour the authigenic development of glauconite through prolonged residence times at the sediment–water interface (i.e., glauconitisation), allowing gradual transformation of smectite precursors into mature glauconitic pellets [28,29]. The depositional setting also influences grain sorting, packing, and the abundance of detrital versus authigenic clay minerals, which in turn affect reservoir quality. Poor sorting and tight grain arrangements inherited from these environments contribute to reduced pore-throat connectivity. This, in turn, increases microporosity, as further described in the next subsection. Consequently, the depositional environment exerts a first-order control on the petrophysical behaviour of greensands, particularly porosity, permeability, and irreducible water saturation (Section 3.2, Section 3.3 and Section 3.4), which are essential for classifying greensand reservoir quality and guiding petrophysical model calibration. Finally, because glauconite functions simultaneously as a framework grain and a conductive clay phase, many standard petrophysical models that assume a strict partitioning between sand and clay fractions are not fully applicable to greensands.

2.3. Microstructure and Dual Porosity

The pore architecture of greensands is notably complex, characterised by a dual porosity system [1,34]. This subsection explores the distribution of macropores and micropores, their petrophysical implications, and challenges for reservoir evaluation.

Macroporosity corresponds to intergranular pore spaces between framework grains, whilst microporosity is mainly controlled by the presence of clay minerals—especially glauconite and chlorite—that create fine networks of isolated pores [34]. Microporosity is generally defined as pores smaller than 0.5 μm [37] and is linked to the high surface area contributed by detrital and authigenic clay minerals.

Figure 3 presents backscattered electron (BSE) images of two greensand samples, with a notable scale bar of 1 μm for micropores. The coexistence of macropores and micropores results in a bimodal pore-throat size distribution (PSD) (Figure 4). These micropores retain bound water, causing high irreducible water saturation [38,39]. This phenomenon presents critical implications for reservoir performance, including fluid storage capacity, flow characteristics, and hydrocarbon recovery strategies.

Figure 3. (a) BSE image of the North Sea greensand; scale bar for greensand is 100 μm, and the image represents macroporosity. Q, quartz; Gl, glauconite; M, mica. (b) BSE glauconite grain image from Arnager greensand; scale bar for glauconite grain is 1 μm. Micropores reside within glauconite grain. Source: Hossain et al. [34]. © Society of Exploration Geophysicists (SEG). Reproduced with permission. DOI: https://doi.org/10.1190/1.3064151.

Figure 4. NMR T₂ curve distribution for greensand samples: (a) T₂ spectra for three Well-A core plugs from a Late Paleocene/Early Eocene sandstone, North Sea [2]; (b) Nini field, North Sea [40]. © Society of Exploration Geophysicists (SEG). Reproduced with permission. DOI: https://doi.org/10.1190/geo2010-0366.1. A peak close to 1 ms represents microporosity, and a peak close to 100 ms represents macroporosity.

Because micropores are often isolated from the macropore network, effective porosity is reduced due to poor pore interconnectivity. However, this pore structure tends to preferentially retain water over hydrocarbons (a water-wet rock), which renders greensands economically viable reservoirs. From a pore-volume standpoint, microporosity largely controls key petrophysical properties such as capillary pressure, porosity, permeability, and water saturation. Additionally, abundant dispersed, laminated, or structurally incorporated clays commonly obstruct pore throats, further reducing effective porosity. This contributes to highly scattered and atypical porosity–permeability trends that differ significantly from those observed in clean sandstones (Figure 5). Such complexity poses considerable challenges for the evaluation and modelling of greensand reservoirs, requiring tailored workflows and calibration strategies to accurately assess reservoir quality.

Figure 5. Total porosity and air permeability cross-plot diagram showing the different trends of clay-free sandstones and greensands [32].

3. Greensand Measurement Challenges

3.1. Mineralogical Analysis

Petrographic analysis using transmitted and reflected light microscopy remains a fundamental tool in the mineralogical characterisation of reservoir rocks. This technique enables geologists to visually examine mineral grains, textures, and their spatial relationships at the microscopic scale. It provides direct insights into the identification of minerals, grain morphology, and diagenetic features, thereby complementing bulk analytical techniques such as X-ray diffraction (XRD). In particular, petrographic observations allow the discrimination of clay minerals based on optical properties such as birefringence, pleochroism, and interference colours, which are often indistinguishable by XRD alone. Furthermore, ternary diagrams plotting the relative proportions of key clay minerals—such as glauconite, chlorite, and smectite—are widely used to classify mineral assemblages and interpret diagenetic pathways in greensand reservoirs [31]. Such a mineralogical framework, integrating petrographic observations and quantitative analyses, supports the evaluation of reservoir quality and geological history by quantifying the relative abundance and interplay between these clay minerals. However, due to the greenish colour imparted by glauconite, these sandstones may be misidentified as containing other clays, such as odinite, clinochlore, or chamosite (all from the chlorite group), and berthierine (from the kaolin group). These minerals like glauconite, typically develop at a slow sedimentary deposition rate [41].

In addition, glauconite can be difficult to identify precisely by XRD because its basal reflections often overlap with those of other 10 Å lattice clay minerals, such as illite and mixed-layer clays [42,43,44,45,46,47]. Recent clay XRD studies have demonstrated that the deconvolution of ethylene glycol-treated samples and the detailed analysis of basal reflections provide a reliable means to distinguish glauconite from mixed-layer silicates, revealing its R3-ordered glauconite–smectite structure with minor expandable layers [31]. Therefore, XRD software tools must be appropriately calibrated to apply such deconvolution techniques effectively and prevent misinterpretation of clay minerals.

3.2. Porosity

Common porosity measurement methods include gas porosimetry based on Boyle’s law—typically using helium or nitrogen; brine porosity, determined by the Archimedes’ method using fully brine-saturated core samples [48]; and nuclear magnetic resonance (NMR) techniques, which measure the transverse relaxation time (T₂) decay [49]. Gas porosimetry accurately measures both connected and microporous pore volumes due to the small molecular size of the gas, although some isolated pores may remain undetected. In contrast, brine porosity measurements can be influenced by the presence of clay-bound and irreducible water [48]. NMR porosity measurements are increasingly used because they can discriminate between fluid types within pore spaces and are non-invasive [50]. Moreover, laboratory technicians should report a drying protocol and a test for residual bound water and discuss the potential underestimation of pore volume when conventional drying is assumed to be complete.

Porosity measurement in greensand reservoirs is complicated by the presence of iron-rich clay minerals and heterogeneous pore systems. Hossain et al. [40] conclude that helium core porosity effectively measures total porosity because the molecular size of this inert gas is small enough to access the micropore network and clay-bound water. In contrast, the Archimedes method, applied to fully brine-saturated core plugs, measures effective porosity since the water molecule is larger than helium and cannot penetrate tightly bound pores. Their core NMR porosity closely matched the brine porosity, with an average absolute error of 2.88 porosity units (p.u.), and was significantly lower than the core helium porosity, with an average absolute error of 3.77 p.u. This finding matches Rueslatten et al.’s [2] studies on oil greensands, since glauconite is paramagnetic due to its iron content, which generates a shortened T₂ relaxation time curve distribution, and it can also lead to surface relaxivity miscalculations for converting the NMR data to a PSD.

Because iron-bearing glauconite produces local magnetic-susceptibility contrasts and strong internal field gradients, empirical adjustments to T₂ cut-off values have to be considered—typically between 10 and 30 milliseconds for oil reservoirs, according to Dodge et al. [1]—which is significantly lower than the conventional sandstone T₂ cut-off of 33 milliseconds [50], but applying these lower thresholds without independent validation risks misclassification of bound versus free fluids when susceptibility-driven relaxation dominates. Empirical T₂ thresholds can mask fundamental signal distortion caused by inhomogeneous magnetic susceptibility; therefore, reliance on such corrections should be stated explicitly as provisional pending physics-based models.

To reduce ambiguity and increase confidence in NMR-based porosity and PSD interpretations of glauconitic greensands, we recommend the following workflow: measure and report bulk magnetic susceptibility for core plugs and cuttings; report full NMR acquisition parameters and justify any T₂ threshold or relaxivity adjustments; calibrate NMR-derived porosity and PSD against independent pore-scale measurements (helium porosity, brine-saturated/Archimedes porosity, MIP, µCT, and core NMR) and report calibration metrics; use complementary tests (comparison of brine and helium porosities, MIP/µCT constraints, and electrical conductivity measurements) to distinguish bound from free fluids; and, where feasible, adopt or test physics-based, susceptibility-aware NMR approaches (field-dependent relaxometry, susceptibility-corrected models, or joint inversions) rather than relying solely on empirical T₂ cut-offs—these steps document the limits of empirical corrections and provide a pathway to more physically consistent NMR interpretations in greensand systems.

3.3. Permeability

Permeability in greensands exhibits highly scattered trends when plotted against porosity, reflecting the complex pore structure and clay distribution (Figure 5). The presence of mixed clay minerals—especially glauconite and chlorite—substantially affects permeability by coating grain surfaces and plugging pore throats, thus reducing interconnected flow pathways. The pore-throat space of a rock can be measured with the specific surface area (SSA), and clay minerals generally display moderate to high SSA values (see Table 2), which correlate with their greater microporosity and lower permeability. Hossain et al. [40] reported a range of SSA from 17 to 23 m²/g through nitrogen adsorption (the SSA of quartz is ~2.5 m²/g) and found an inverse relationship with the macroporosity and permeability. Hossain and Zhou [51] show a relationship between porosity and permeability, with the SSA discriminated by the greensand’s pore-filling clay distribution.

Table 2. Cation-exchange capacity range and total surface area for clay minerals (from Navarro-Perez et al. [52]; adapted from Van Olphen and Fripiat [53]; McPhee et al. [48]).

Clay Mineral Group	CEC (MEQ/100 g)	Surface Area (m2/g) 1
Smectite	70–130	800
Illite	25–40	30
Chlorite	10–40	15
Kaolinite	3–15	15

¹ Summation of internal (interlayer) and external surface area.

Several researchers have developed innovative methodologies to determine the permeability of greensand in the subsurface by calibrating well-log data using core measurements. The discrimination of iron content, rock matrix density, and NMR parameters is important to define an optimised permeability prediction. Table 3 summarises the main permeability equations in the literature used for greensands. The Kozeny, Timur–Coates, and SDR equations are most frequently applied, either in their classical or modified style. The latter two, NMR-based permeability models, have been developed to integrate relaxation and diffusion properties; these approaches show promise for more reliable permeability estimation in clay-rich reservoirs by accounting for pore-size heterogeneity and clay influence. Further information on the methods for permeability estimation for greensands in the literature is displayed in Table 4. Moreover, permeability predictions based on total SSA must be reconsidered in glauconitic systems because a portion of the surface is associated with hydraulically ineffective microporosity and bound water; models using Kozeny require filtering or redefinitions in their inputs.

Table 3. Permeability equations applied for greensand reservoirs.

Name	Equation	Reference
Timur and Coates (TC)	$k={\left({\varphi }_{NMR}\right)}^4{\left(FFI/BVI\right)}^2$	[54]
Schlumberger–Doll (SRD)	$k=4.5{\left({\varphi }_{NMR}\right)}^4{\left(T_{2.g}\right)}^2$	[55]
Kozeny	$k=c{\displaystyle \frac{{\varphi }^3}{S^2}}$	[56]
Modified Kozeny’s to include macroporosity range	$k=c\varphi {{\rho }_2}^2{\displaystyle \sum _{i=1}^N}{f}_i{\left(T_{2i}\right)}^2$	[40]
Worthington’s modified Kozeny’s equation	$k={\left({\displaystyle \frac{B}{F}}\right)}^{1/C}$	[57]
Modified Kozeny’s as a function of rock type	$k=c{\displaystyle \frac{{\varphi }^{3-2a}}{{10}^{2b}}}$	[51]

Nomenclature: $k$ = permeability (mD), ${\varphi }_{NMR}$ = NMR porosity (v/v), $FFI$ = NMR log free fluid index (v/v), $BVI$ = NMR bulk volume irreducible fluid (v/v), $T_{2.g}$ = geometric mean of T₂ distribution time (ms), $c$ = Kozeny’s constant, $S$ = specific surface area of bulk (1/μm), ${\rho }_2$ = surface relaxivity (μm/ms), $f_i$ = fraction of the total amplitude of each $T_{2i}$, $F$ = electrical formation factor (F = a/ϕ^m); $B$, $C$, $a$, and $b$ are fitting constants.

Table 4. Permeability estimation methods found in the literature review used on greensand reservoirs.

Method	Comments	Ref.
Log NMR permeability with SRD and Timur–Coates (TC) equations.	Iron content underestimates NMR-derived permeability for the TC equation; care must be taken to define the T2 cut-off value. The fitted factors of the formulas used were enough for good calibration. Suggested T2 cut-off values according to the iron content in greensand reservoirs.	[1]
Electrofacies pattern linked to permeability transforms algorithm using core porosity and permeability.	Log synthetic permeabilities used as input were litho-density, neutron, sonic, and gamma-ray spectrometry logs. Grouping the electrofacies (lithological units) is extremely important.	[58]
NMR permeability with the Timur–Coates equation.	T2 cut-off values below 10 ms for chloritic greensands and 33 ms when chlorite and glauconite are present (oil production).	[2]
Log NMR permeability with the Timur–Coates equation.	Chlorite presence influences the irreducible bulk volume when using the TC equation. Density-derived porosity log replaced the FFI/BVI term in the TC formula, increasing permeability estimation.	[38]
Artificial neural network technique to estimate permeability.	147 log response sets were trained with core permeability from eight wells. The synthetic permeability log shown as an example gave good consistency results.	[15]
Density Constrained Stochastic Modelling (DCSM).	Method based on a random selection of core bulk density values matched with an apparent matrix density log. The average density tolerance between the two parameters is less or equal to 0.05 g/cm3.	[17]
Modified Kozeny’s equation to include the whole macroporosity range of T2 times.	Kozeny’s factor, C = 8.3, was estimated from the Mortensen et al. porosity model. Surface relaxivity derived from specific surface area from Kozeny’s BET and image analyses. The BET-specific surface area takes into account the microporosity range, while the image and Kozeny’s specific surface area are associated with the macroporosity range.	[40]
Empirical correlation of permeability with the electrical formation factor—Worthington’s modified Kozeny’s equation.	The formation factor was estimated using the equation F = a/ϕm, with a = 1.67 and m = 1.9. A linear relationship between permeability and formation factor was found by varying the specific surface area. The diagenesis of greensands needs to be known to replicate this method.	[57]
Modified Kozeny’s equation by including two factors, a and b, dependent on the rock type, instead of the specific surface area or surface relaxivity, and as a function of porosity.	Factors a and b are constants derived from a linear relationship between the specific surface area and porosity. For clean sandstone, a = −1.0 and b = 2.2; for clay-bearing sandstone, a = −2.5 and b = −2.3. For greensand with pore-filling cementation, a = −5.5 and b = 3.0. A linear relationship between Kozeny’s constant, c, and porosity is proposed.	[51]

3.4. Irreducible Water Saturation

Since greensands have a complex microstructure due to the presence of clay, it is expected that the irreducible water saturation (S_wirr) and the capillary pressure curves will be high (Figure 6). The glauconitic grains are water-wet [16], favouring storing water in the micropore range and leaving hydrocarbon in the macropore range (Figure 7). Table 5 summarises reported values for the irreducible water saturation in greensands, with values of up to 78% v/v, according to the literature.

Figure 6. Capillary pressure and water saturation cross-plot comparing clay-free sandstone and greensand trends [32].

Figure 7. NMR T₂ distribution diagram comparing clay-free sandstone and greensand distributions [32].

Table 5. Irreducible water saturation values found in greensands worldwide along with the technique used to define them.

Swirr Range 1 (%v/v)	T2 Cut-Off Value (ms)	Technique Used	Ref.
12–78	10 to 30	Centrifuge air/brine drainage capillary pressure and NMR T2 distribution.	[1]
27–55	33	Decane–brine saturation, Karl Fischer titration, and NMR T2 distribution	[2]
27–41	33 and 10 for chlorite zones	Karl Fischer titration and NMR T2 distribution	[38]
22–41	5.2 and 3.7	Centrifuge air/brine drainage capillary pressure and NMR T2 distribution.	[40]

¹ S_wirr is irreducible water saturation.

As previously stated in Section 3.2, the iron content in greensands affects the NMR T₂ readings and hence the estimated S_wirr; that is why the authors mentioned in Table 5 used lower T₂ cut-off values. Dodge et al. [1] suggest that the T₂ cut-off value needs to be lower than 10 ms to quantify S_wirr [38]. Typical T₂ cut-off values of 33 ms for free mobile fluid and 3 ms for clay-bound water for greensand reservoirs are incorrect for greensands. The T₂ decays faster due to the iron paramagnetic properties and narrower pore-size distribution; thus, the T₂ cut-off value must be lowered (e.g., [59]). Hossain et al. [40] went further, and using the capillary pressure curves, they defined a cut-off value of 100 psig to separate the microporosity from the meso- and macroporosity zone equivalent to a T₂ cut-off value of 5.21 ms.

Furthermore, the gas–water permeability curve for greensands is expected to shift to the right (Figure 8) owing to the high S_wirr and its microporosity portion. The water relative permeability curve will start at a moderate to high S_wirr and effectively flow from 2% of k_rw onwards [60]. In comparison, the gas relative permeability curve will start at 100% k_rg and reach a small value of residual gas saturation (1-S_rg), where the remaining hydrocarbon gets trapped.

Figure 8. Gas–water relative permeability and water saturation cross-plot comparing the trend of clay-free sandstones (continuous line) and greensands (dashed line). K_rg is gas relative permeability, K_rw is water relative permeability, S_wirr is irreducible water saturation, and S_rg is residual gas saturation [32].

3.5. Water Saturation Modelling

Greensands often have high rock conductivity due to the significant cation-exchange capacity of glauconitic grains. Weaver [61] reports values from 5 to 12 meq/100 gr for glauconites with up to 5% expandable clays, and with 50% expandable layers, CEC values reach up to 40 meq/100 gr. Patchett et al. [8] reports values from 7.8 to 32.4 meq/100 gr (13 to 81% glauconite). In contrast, values for greensand deep resistivity logs range from 1 to 5 ohm·m [19,38,62]. Since these values are low, a reservoir can be confused with freshwater rather than a hydrocarbon zone.

Greensands are referred to as low-resistivity pays, according to the definition by Worthington [63] (p.78): “a lack of useful positive contrast in measured electrical resistivity between zones that contain and produce hydrocarbons in commercial quantities and zones that contain and produce only water, within the same reservoir system”. Sneider [64] uses the term “low-resistivity, low-contrast” (LRLC) to refer to sandstones with very low resistivities (<2 ohms·m) that have low contrast in resistivity with adjacent shales. Excess clay minerals, fine grains, and microporosity are some of the leading causes of low-resistivity pays, which are features of greensands.

Archie [9], Waxman–Smits [11], and Simandoux [65] are the three models used frequently for greensands worldwide (Table 6 and Table 7). Waxman–Smits is the main representative of the double-layer models and uses the cation-exchange capacity parameter. Simandoux represents Vsh models since it adds a shaley term. The Vsh models are based on the wetted-shale/clay volume fraction, meaning that they implicitly assume that the electrical properties of clays, independent of how they are distributed in sandstones, are the same as the layers of the detrital clay adjacent to the sandstones. The advantage of using them is that shale/clay parameters can be estimated from log data alone [10].

Table 6. Water saturation models used on greensands from literature.

Location	Model	Ref.
Trimble Field, MS, USA	Pseudo-Archie using m = 1.8 and n = 1.77	[63]
Nini Field, North Sea	Pseudo-Archie using a = 1.67, m = 1.18, n = 2.4 and Rw = 0.077 ohm·m.	[66]
Trembul Field, Indonesia	Waxman–Smits using a = 1.0, m = 1.76, n = 1.79 and Rw = 0.19 ohm·m @148 °F.	[19]
Glauconite Formation, Southern Chile	Simandoux using a = 1, m = 2.09, n = 1.66.	[67]
Magallanes Formation, Southern Argentina	Pseudo-Archie using a = 0.8–0.82, m = 1.4–1.6, n = 1.4–1.6 and Rw = 0.3 ohm·m @150 °F.	[68]

Table 7. Water saturation models expressed in conductivity terms used in greensands.

Model	Equation	Ref.
Archie	$C_t={\displaystyle \frac{C_w{\varphi }^m{S_w}^n}{a}}$	[9,69]
Simandoux	$C_t={\displaystyle \frac{C_w}{F}}{S_w}^n+V_{sh}{C}_{sh}$	[62,65]
Waxman–Smits	$C_t={\displaystyle \frac{C_w}{F^{\ast }}}{S_w}^n+{\displaystyle \frac{{BQ}_v}{F^{\ast }}}{S_w}^{n-1}$	[10,11]

Nomenclature: $S_w$ = water saturation (v/v), $C_w$ = water conductivity (S/m), $C_t$ = true rock conductivity (S/m), $F$ = Archie formation factor, $a$ = tortuosity factor constant, $\varphi$ = porosity (v/v), $m$ = Archie cementation exponent, $n$ = Archie saturation exponent, $F^{\ast }$ = apparent formation factor, $Q_v$ = cation-exchange capacity per unit pore volume (meq/mL), $B$ = equivalent conductance of clay (mho·ml/(meq·m)), $C_{sh}$ = shale conductivity (S/m), $V_{sh}$ = shale or clay volume (v/v).

The double-layer models offer a better scientific understanding of the rock’s electrical behaviour. However, they require core data to calibrate their terms, such as Qv, for log-derived parameters (e.g., [48]). It is important to note that these water saturation models—Archie, Simandoux, and Waxman–Smits—do not use glauconitic sandstones as empirical data for their postulates, so care should be taken when applying them to other rock-type reservoirs such as greensands.

4. Impact of Greensand Well Logs

The interpretation of well logs in greensand reservoirs poses significant challenges due to their complex mineralogical and petrophysical characteristics (see Table 8). A prominent issue is the notably high gamma-ray response, primarily attributed to the elevated potassium content in glauconite. This can be misinterpreted as shaliness, resulting in overestimation of clay volume if standard clay or shale cut-offs are applied. Spectral gamma-ray logs are especially valuable where available. In particular, K/Th ratios combined with the photoelectric factor log can be employed to identify glauconite [70].

Table 8. Summary table showing how greensand affects well-log readings and which petrophysical properties are consequently under- or overestimated.

Well Log	Greensand Effect	Causes	Petrophysical Estimation	Reference
Gamma-ray	Higher response than clean and shaly sandstone.	High presence of potassium. Greensands can contain other clay minerals, such as chlorite, siderite, and pyrite. Higher boron content than other clay minerals.	The shale or clay volume calculated is overestimated.	[17,27,35]
Deep resistivity	Lower response similar to freshwater zones.	High cation cation-exchange capacity (CEC), meaning lower resistivity. Large amount of bound water in the glauconitic grains.	The hydrocarbon zone is not easily identified. The water saturation is overestimated.	[8,35,71]
Neutron porosity	Higher response than sandstone.	Large thermal neutron absorption cross-section because of its high iron content. Higher boron content than other clay minerals.	Neutron porosity is overestimated.	[8,17]
Bulk density	Higher response than sandstone.	Glauconite is denser than sandstone. Iron presence.	Density porosity is underestimated.	[8,17,25,71]
Photoelectric factor	Higher response than sandstone.	Relatively high molecular weight. Iron presence.	It can be used to identify the glauconitic sandstone lithology.	[8,35]
NMR tool	T2 decays faster.	Paramagnetic effect of the iron content of greensand.	Bulk mobile fluid underestimated. T2 cut-off value needs to be lower than 30 ms.	[1,2,38]

Due to the greensand effect observed in well logs, core analysis is essential for reliable calibration and petrophysical model development. For example, as shown in Figure 9, the Hermod and Ty formations display the lowest resistivity readings and minimal density–neutron separation, even though core helium porosity and permeability indicate that these intervals remain permeable (permeability greater than 200 mD) and porous (porosity between 38 and 43% v/v).

Figure 9. Nini-1 well logs showing the greensand reservoirs intervals (Hermod and Ty sands from the North Sea): (a) gamma-ray log; (b) porosity logs: bulk density, neutron porosity, and helium porosity from core analysis; (c) resistivity log; and (d) permeability log (using Kozeny’s equation) from core analysis [26].

Figure 10 presents a schematic summary of typical well-log responses, illustrating the gas effect in clay-free sandstones (neutron–density crossover) and its absence in greensands. Electrical resistivity logs often produce deceptively low values in glauconitic formations. The high cation-exchange capacity of clay minerals, together with clay-bound and capillary-bound water, enhances the rock’s electrical conductivity, resulting in resistivity readings that may underestimate hydrocarbon saturation and complicate petrophysical interpretations.

Figure 10. Diagram of conventional well-log responses in quartz sandstone and greensand formations, from left to right: gamma-ray log (GR), deep resistivity log (Rdeep), neutron log (NEU), bulk density log (DEN), and photoelectric factor log (PEF) [32].

Neutron logs tend to overestimate porosity and fluid content due to the significant hydrogen content in iron-rich clay minerals and the associated bound water. Conversely, bulk density logs frequently underestimate porosity, as the higher density of glauconitic and chloritic minerals biases measurements upward. The increased mineral density thus reduces calculated porosity when standard matrix density values are used.

Nuclear magnetic resonance (NMR) logging underestimates mobile fluid volumes because iron-bearing clays increase surface relaxivity, causing rapid decay of NMR signals—seen as shorter T₂ relaxation times. Combined with the dominance of microporosity-hosted fluids, this impedes effective discrimination between movable and bound fluids if conventional T₂ cut-off values are used [1,2,38].

5. Interpretation Framework for Greensand Reservoirs

5.1. Greensands’ Petrophysical Controls

The literature identifies four key controls (Figure 11) that underpin porosity, permeability, water saturation, and electrical behaviour in these formations. These controls are interrelated and manifest at both the grain and pore scale, shaping the overall petrophysical signature of greensands. First, the presence of glauconite and associated clay minerals, including chlorite and illite/smectite, exerts a dominant influence. These minerals may be embedded in the framework or occur as pore linings and fillings, directly contributing to heterogeneity in rock texture and anisotropy in physical properties. This mineralogical composition modifies lithological identification, pay zone identification, and permeability characterisation. Their distribution influences grain packing, introduces paramagnetism, and reduces the reliability of standard well-log interpretation techniques.

Figure 11. Conceptual framework of petrophysical controls in greensand formations as identified through literature review [32].

Second, microporosity—often defined by pore-throat diameters smaller than 1 μm—is a ubiquitous feature in glauconitic grains. These micropores frequently lack connectivity with macropores, reducing effective porosity and flow potential. However, they preferentially retain water over hydrocarbons due to strong capillary forces and water-wet rock conditions. Thus, microporosity impacts reservoir quality, fluid distribution, and S_wirr estimations. Third, the specific surface area (SSA) of greensands is high due to the abundance of fine-grained clays and poorly sorted textures. SSA is directly proportional to microporosity and inversely related to permeability and porosity. This relationship challenges upscaling efforts from core to log data and contributes to misleading poro–perm correlations unless mineralogy is explicitly considered.

Fourth, electrical conductivity induced by clay minerals introduces a secondary current path in resistivity measurements. These conductive clays react electrochemically with formation water, particularly under low-salinity conditions, through cation-exchange mechanisms. The presence of glauconite, which exhibits a moderate to high CEC, increases this conductivity and distorts resistivity-derived saturation calculations. As a result, models based on Archie’s law tend to overestimate S_w unless compensated with shale/clay-based models such as Waxman–Smits or Simandoux. These four petrophysical controls—mineralogical heterogeneity, microporosity, high SSA, and clay conductivity—must be accounted for in any reliable interpretation workflow for greensand reservoirs. Neglecting them not only compromises reservoir characterisation but also affects volumetric estimates, net pay quantification, and ultimately development decisions.

5.2. Interpretation Workflows and Tool Recommendations

Interpretation workflows in greensand formations must begin with a careful selection of tools that respond appropriately to their mineralogical and pore-scale complexity. Table 9 outlines these challenges and offers recommended approaches across four categories: (1) lithology identification, (2) porosity estimation, (3) saturation and electrical properties, and (4) permeability determination.

Table 9. Challenges and recommended tools for reservoir property estimation in greensands [32].

Reservoir Property	Challenge	Recommended Tool/Approach (Including Core-Based Methods)
Porosity	Microporosity retention; poor intergranular sorting	NMR (adjusted T2 cut-offs), brine–helium porosity comparison, SEM image calibration
Permeability	Pore-throat obstruction by glauconite and chlorite; poor sorting	NMR-based models (Timur–Coates, SDR), SSA estimation, core–log regression
Saturation	Overestimated Sw from resistivity; non-Archie behaviour	Waxman–Smits or dual-water models; field-calibrated m and n; CEC measurement
Clay Volume	GR over-response due to high K; mineral misidentification	Spectral gamma-ray, PEF logs, clay typing via mineralogical analysis (XRD, SEM)
Rock Typing	Electrofacies overlap; textural heterogeneity	Multi-mineral log inversion; unsupervised clustering; thin-section validation
Net Pay Determination	Inconsistent cut-offs for Swirr and porosity	NMR calibration, capillary pressure curves, core-calibrated net pay criteria
Reservoir Quality Mapping	Misleading poro–perm trends; variable Swirr	Integration of digital rock physics, electrofacies models, and cross-plots
Logging Environment	High sensitivity to salinity, temperature, and iron content	In situ environmental corrections, formation-specific interpretation templates

Note: While advanced techniques such as NMR and digital rock analysis are highlighted, core-based methods—including Archimedes (brine saturation) and gas porosimetry—remain valuable for porosity estimation and are often more cost-effective in early-stage reservoir evaluation.

Lithology identification in greensands is complicated by the response of gamma-ray and density–neutron logs to glauconite and other clays. Traditional indicators like spontaneous potential and gamma-ray logs are influenced by high potassium and iron contents, often leading to lithological misclassification. To improve discrimination, tools such as the photoelectric factor (PEF) and spectral gamma-ray logs are recommended. Elemental spectroscopy tools like ECS (Elemental Capture Spectroscopy) offer further refinements by quantifying elemental composition, including iron, silicon, and potassium, which can distinguish glauconitic from other clay-rich zones [71]. Integrating core mineralogy with these logs significantly enhances lithological models. However, defining petrofacies remains challenging due to scattered porosity–permeability trends. Capillary pressure curves and pore-size distribution (PSD) analysis can help clarify pore-throat geometries, and acoustic logs may serve as proxies for reservoir quality in texturally heterogeneous intervals [25].

Porosity estimation is equally complex due to the bimodal distribution and high microporosity in glauconitic sands. Conventional porosity logs—neutron, density, and sonic—must be calibrated against core porosity data, preferably derived from helium expansion or brine saturation methods. NMR tools such as CMR (Combinable Magnetic Resonance) can characterise free-fluid and bound-water volumes and differentiate pore systems. However, the paramagnetic effect of glauconite—due to its iron content—shortens T₂ relaxation times, requiring careful adjustment of cut-off values to avoid underestimating mobile porosity [1,2]. To strengthen interpretation, complementary laboratory techniques such as mercury intrusion porosimetry (MIP) and micro-computed tomography (µCT) are recommended, as they provide independent pore-size distribution data and can help validate NMR-derived porosity estimates. In some cases, µCT may also assist in estimating glauconite content if density contrast permits.

Saturation and electrical properties are strongly affected by clay conductivity and water-wet rock behaviour. Greensands often require modified saturation models, such as Waxman–Smits or Simandoux, since Archie’s model typically underestimates Sw due to the additional conductive path introduced by clays. Core-based measurements of cation-exchange capacity (CEC), multi-salinity tests, and capillary pressure curves (e.g., mercury injection capillary pressure, MICP) are vital for calibrating saturation models. These measurements reveal elevated irreducible water saturation and steep capillary pressure profiles, both of which reflect the dominance of micropores in storing formation water [47].

Permeability estimation also demands a combined approach. While NMR-based models such as Timur–Coates or SDR provide log-derived permeability estimates, their accuracy is limited in greensands without calibration. The presence of pore-blocking authigenic clays and cementation reduces pore-throat connectivity, often leading to significant permeability impairment, particularly under low-salinity conditions where clay swelling or migration may occur. Laboratory-determined gas or brine permeability remains essential for ground-truthing log responses. Empirical models, including Kozeny’s [57] equation, must be applied cautiously, with a clear understanding of their assumptions and limits.

Finally, geomechanical logging—derived from acoustic and sonic data—can further refine reservoir quality interpretation. These measurements provide information on elastic properties, fracture propagation, and rock brittleness, offering additional insight into stress sensitivity and completion design. In moderately to well-consolidated greensand units, P-impedance and acoustic velocity data can effectively discriminate between productive and non-productive intervals [25].

6. Conclusions and Perspectives

In this review, we synthesised extensive research on the petrophysical controls governing greensand reservoirs, emphasising their distinct mineralogical and pore-scale complexities. Our study confirms that glauconite and associated clay minerals significantly influence porosity, permeability, and water saturation measurements, often leading to challenges in conventional well-log interpretation and reservoir characterisation.

Traditional petrophysical models commonly applied to sandstones frequently fail to accommodate the paramagnetic and conductive effects imparted by glauconite’s iron content and high cation-exchange capacity. This commonly results in over- or underestimation of key reservoir parameters, such as porosity and fluid saturations, when standard log interpretations are used without tailored calibrations. Consequently, core analysis remains an indispensable tool for validating log-derived petrophysical properties and developing robust interpretation frameworks.

To improve reservoir evaluation accuracy in greensand contexts, it is important to recognise that glauconite behaves as a conductive, microporous framework mineral with significant magnetic susceptibility and bound water. Integrated workflows are therefore recommended, combining spectral gamma-ray, NMR with provisional adjusted T₂ cut-offs validated against independent measurements, and shale–sand saturation models like Waxman–Smits or Simandoux, calibrated against core and laboratory data from core NMR, MICP, CT, and XRD/mineralogical analysis. These combined approaches help mitigate the misleading effects caused by glauconitic minerals and fine clays, thereby enhancing pay zone identification and net reservoir quality assessments. We also recommend explicit testing of model assumptions and mandatory reporting of key supporting data, including XRD-derived mineral fractions, petrographic modal analysis, bulk magnetic susceptibility, drying protocol, and the rationale for any empirical T₂ or relaxivity adjustments, before applying standard petrophysical models.

Looking forward, future research should prioritise comprehensive core–log–digital rock physics integration to better quantify the impact of mineral heterogeneity and diagenesis on reservoir properties. The development of rock-typing algorithms and machine learning workflows tailored specifically to greensand mineralogy and pore systems holds promise to refine petrophysical models further. Additionally, examining the influence of geochemical and environmental factors on glauconite stability and reservoir quality will support improved predictive capabilities under variable production conditions.

Given the increasing exploration interest in greensand reservoirs worldwide, greater collaboration between academia, industry practitioners, and technology innovators is essential to evolve interpretation standards and deploy best practices. By embracing the unique petrophysical nature of greensands and advancing specialised tools and workflows, the petroleum sector can enhance hydrocarbon recovery efficiencies and optimise reservoir management in these complex lithologies.