1 Introduction

Generally, aeromagnetic data have been utilized in exploring and recognizing mineralization districts, hydrocarbon exploration, geothermal activity, archaeology site investigations, and engineering applications [1,2,3,4,5,6,7,8,9,10,11].

These data have delivered significant information at various levels of detail, extending from contacts among zones and layering within zones to faults-controlled intrusive dykes that can affect the mine planning [12,13,14,15]. Furthermore, the aeromagnetic measurements have the benefit of being able to quickly cover difficult to access areas covering a wide range [16,17,18]. Recently, magnetic data interpretation has been done using methods that include simple geologic models and magnetic gradients parameters to recognize the shallower and deeper structures and distinguish the structure features, which control the mineralization zones [19,20,21,22,23,24,25].

This article deals mainly with delineation and elucidation of the structures that controlled the mineralization zones utilizing the airborne magnetic and the gamma-ray aero-spectroscopy records in the exposed Neoproterozoic rocks of the Gabel Umm Tineidba and its environs, South Eastern Desert, Egypt (Fig. 1). The whole district is regionally covered by exposures such as gneisses, migmatites, ophiolitic mélange, metavolcanics, younger granites, and Quaternary sedimentary covers. The total magnetic data were processed and elucidated using several techniques such as a reduced-to-pole (RTP), radially average power spectrum (PS), analytical signal (As), tilt-angle (Tg), and local wavenumber (LW) to reveal the tectonic and geological structures that are required to locate possible uranium, gold, and sulfide-rich mineralization zones. By using the above-mentioned methods, it permits mapping of the economic mineralized zones and their associated-structures.

Fig. 1
figure 1

The location and the geological map of Umm Tineidba area, Southern Eastern Desert, Egypt [30]

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2 Geological Backgrounds

The study area is part of the Neoproterozoic Arabian-Nubian Shield (ANS) fluctuating in age from 900 to 550 Ma. The ANS can be characterized by a complex amalgam of arc, ophiolite, and micro-continental terranes that resulted from the Neoproterozoic closure of the Mozambique Ocean [26,27,28,29,30]. Three chief Neoproterozoic rock units involving gneisses and migmatites, dissected ophiolites/ophiolitic mélange, and island arc volcano-sedimentary rocks have been described in South Eastern Desert, Egypt [31, 32]. Younger gabbroic to granitic intrusions invade the three units underlying Quaternary deposits (Fig. 1).

2.1 Gneisses and Migmatites

These rocks occupy more than half of the exposed rocks. Their outcrops occur as uplifted domal old rocks and encompass gneisses, metagabbros-diorites, migmatites, and meta-sedimentary and volcano-sedimentary sequences displaying polyphases of deformations [33]. These rocks are delimited by a complex array of thrust faults trending generally in NE–SW, separating them from folded thrust belts of ophiolitic mélange in the east and metavolcanics in the west. Many authors assigned the ages of these gneisses as pre-Neoproterozoic (> 900 Ma) [34] or Pan-African (900–850 Ma) [35, 36].

2.2 Ophiolitic Mélanges

Ophiolitic mélanges are well exposed in the northeastern and southern parts of the studied province. They occur as E–W elongated exotic blocks embedded in foliated sedimentary matrix [37]. NE–SW and NW–SE-trending folds related to NNW–SSE shortening have been observed [38]. Intraoceanic back-arc to volcanic arc tectonic regime has been proposed for the origin of these rocks [39]. The age of ophiolitic mélange was detected at almost 870–740 Ma [40].

2.3 Island Arc Metavolcanics

These sequences cover ~ 10% in the western part of the investigated area, uncomfortably overlying the genesis rocks. Metabasalts, metaandesites, metadacites, and their equivalent metapyroclastics with banded iron formation and marble are the main varieties of these volcanic rocks [41]. These rocks are circumscribed by two chief fault thrusts trending in E–W and NNE, plunge toward the NW. Furthermore, in the NW–SE, their trending folds are influenced by penetrating metamorphism [42]. An age of 813 ± 6 to 615 ± 6 Ma has been assigned to the island arc metavolcanics [43, 44].

2.4 Younger Granites

These rocks are broadly distributed in the investigated region. Their landform forms sharp intrusive contacts with surrounding rock units. They are leucocratic-mesocratic, coarse-grained, red in color, and show compositional range from alkali feldspar granite to syenogranite. Their rocks types enclose numerous xenoliths involving gneissic, ophiolitic, gabbro, and metavolcanic blocks derived from the underlying rocks. The rift-related younger granites have been assigned to 590–550 Ma [45,46,47].

2.5 Quaternary Deposits

Quaternary deposits are represented by alluvial sediments. The latter are widely distributed in the southern portion of the investigated region such as Wadi Umm Ghalqa, Wadi Haimur, Wadi Bitan, and Wadi Abo Had [48].

Structurally, the examined area is exaggerated by two principal shear zones trending NE and NW. The latter trend is considered as a part of the Najd fault system consisting of a brittle-ductile zone, which has a width of 300 km and extends to 1100 km in length, spreading through the northern portion of the ANS [49, 50]. These shear zones cross the Pan-African ophiolitic mélange, island arc, and numerous intrusive rocks to the east. There are folds and faults, recorded within these shear zones. The former is mainly open asymmetrical anticlines with axial planes striking NE and the limbs dip steeply at about 70° and 60° NW and SE, respectively. These folds mainly plunge more than 80° to the S40° W direction. They mainly affect the island arc metavolcanics and their metapyroclastics (crystal metatuffs) that arise in the northwestern portion of the examined area. Thrust, strike-slip, and normal faults are recorded in the area under investigation, cutting through the ophiolitic mélange and subducted-related volcano-sedimentary rocks (Fig. 1). These faults trend in the ENE–WSW to E–W and dip steeply to the NW. All fault thrusts in the investigated area are analogous to the major axial plane of fold, which happens in the northern part of the area under examination.

3 Data Usability

The aeromagnetic and aero-radio-spectrometric data were obtained over the investigated area among latitudes 22° 45'N and 23 o 00'N and longitudes 33° 50'E and 34° 40'E by the Aeroservice company [51]. The survey flight lines constructed with spacing of 1000 m between each lines and the tie-lines spacing was 10,000 m perpendicular to flight lines direction (NE–SW). The attained magnetic and the gamma-ray spectroscopy data are reduced, gathered, and lastly offered in the outline of contour and composite maps.

4 Magnetic Data Processing and Interpretations

The magnetic data were preprocessed and corrected for latitude, diurnal variation, and height issue and the total aerial magnetic map (Tm) of the investigated area was created (Fig. 2). Figure 2 reveals that the Tm-values range from 42,350 to 42,638 nT. Magnetic values can be organized into various colors, as indicated by their amplitudes. First, the blue color shades ranging from 42,350 to 42,420 nT are categorized by low magnetic anomalies, with extended and striking in the NE–SW. The intermediate-scale colors range from 42,420 to 42,500 nT, and mostly cover the southern and the eastern parts. Also, the high amplitude, which ranges from 42,500 to 42,638 nT covers the midpoint of the examined area and strike in the NE–SW trend (Fig. 2).

Fig. 2
figure 2

The total magnetic (Tm) map of Umm Tineidba area, Southern Eastern Desert, Egypt [51]

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4.1 Reduced-To-Magnetic Pole (RTP)

Baranov [52] was the first one who introduced reduced-to-magnetic pole (RTP). RTP is an important part of magnetic data processing, especially for large-scale mapping. RTP is intended to remove the skewness of the anomalies and make it symmetric over the source which is magnetized by induction only, remove influence of magnetic latitude, and reduce the effect of dip magnetization, remove the effect of remnant magnetization. Therefore, the Tm-map (Fig. 2) has an embedded impact of latitude discrepancy because of the dipole of the magnetic field. To decrease this influence, the Tm-data was changed to an unreal position as in the pole of the earth and this permits a good accurateness in the site of the inferred anomalies [52,53,54,55,56,57].

The RTP-map (Fig. 3) was accomplished relying on the Earth total intensity (42,470 nT), magnetic field inclinations (32.8° N) and declination (1.9° E) of the survey at the location. The RTP-map does not differ completely from the Tm-map, but a few anomalies alter their trend northward through the elimination of the declination of the investigated area (Fig. 3). The magnetic magnitudes in the exanimated area are circulated intermittently through the lithological variety in the investigated zone and, furthermore, with the manifestation of a sedimentary cover to the south. The RTP-map indicates that the study area is described by an extensive variety of magnetic values ranging from 60 to 185 nT. The RTP highest amplitudes (red shading, which characterized the high magnetic anomalies; RTP-H1 to RTP-H10 zones) are sited in the northern, northwestern, northeastern, and south-southeastern portions and directed to the NE–SW, N–S, and NW–SE trends of the inspected area. Likewise, the lowest values (blue shading, which characterized the low magnetic anomalies; RTP-L1 to RTP-L11 zones) of − 75 to − 110 nT reading are found in the northeastern, southwestern, and northwestern parts and striking in the NE–SW directions in the area under study.

Fig. 3
figure 3

The reduced-to-pole aeromagnetic (RTP) map of Umm Tineidba area, Southern Eastern Desert, Egypt

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4.2 Power Spectrum (PS)

The power spectrum (PS) method was utilized to segregate the local (residual) and global (regional) magnetic fields, detect the depths of shallow and deeper structures, and delineate subsurface geologic structures [58,59,60,61]. This method uses the fast Fourier transform. Therefore, a 2D power spectrum curve was attained (Fig. 4). The slopes of the portions yielding the depth evaluation for magnetic sources were calculated. The depth (z) for every source outfit in charge of each segment was figured by presenting the slope of this part in the formula:

Fig. 4
figure 4

The power spectrum curves of the reduced-to-pole aeromagnetic (RTP)-map of Umm Tineidba area, Southern Eastern Desert, Egypt

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$$z=\frac{-slope}{4\pi}.$$
(1)

Moreover, the depth is evaluated from the slope of the plot between the logarithmic power spectrum and wavenumber (Fig. 4). The radially averaged power spectrum of the magnetic spectrum can be interpreted as two linear slope segments and has been applied to estimate the depth of magnetic interface at 1750 m and 300 m, which represent the average depth to the lower and upper surface of the magnetized body (Fig. 4). Also, the residual and regional magnetic maps, which represent the near-surface and deep-seated structures, were presented by implementing the power spectrum procedure on the aeromagnetic map (Figs. 5 and 6, respectively). Figure 5 exhibits the residual magnetic map, which lacks the subterranean crustal inhomogeneity, and shows various positive and negative anomalies, and some of them are striking in the NE–SW direction (majority), as well as N–S and NW–SE. Also, the high magnetic values are given in Fig. 5 (RES-H) and values range between 10 and 54 nT. In contrast, the lower values are represented by symbol RES-L and range from − 20 to − 55 nT. Meanwhile, Fig. 6 shows the regional magnetic map and map portrays the main subsurface patterns that influence the deep-seated structures and their depths vary between 300 and 1750 m. This map describes two main sets of structures trending in the NE–SW and NNE–SSE, which represent the highest regional anomalies (REG-H1 to REG-H8) and their values range from 60 to 145 nT while the lowest regional anomalies values (REG-L1 to REG-L9) range from − 63 to − 90 nT (Fig. 6). Even as these patterns are overwhelming on this map, the nearness of the short NW–SE and E–W trending faults are likewise significant.

Fig. 5
figure 5

Residual aeromagnetic anomaly map of Umm Tineidba area, Southern Eastern Desert, Egypt, and the black lines represent the interpreted lineament trends

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Fig. 6
figure 6

Regional aeromagnetic map of Umm Tineidba area, Southern Eastern Desert, Egypt, and the black lines represent the interpreted lineament trends

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4.3 3D Analytical signal (As)

Magnetic elucidation was achieved utilizing an adapted method, established totally on the simplification of the analytical signal (As technique) in 3D. Roset et al. [62] precisely defined the absolute amplitude value of the 3D analytical signal as follows:

$$As=\sqrt{{\left(THDR\right)}^{2}+{\left(VDR\right)}^{2}},$$
(2)

where \(VDR=-\frac{\partial T}{\partial z}\) is the vertical derivative of the magnetic field in the direction of z and

$$THDR=\sqrt{{\left(\frac{\partial T}{\partial x}\right)}^{2}+{\left(\frac{\partial T}{\partial y}\right)}^{2}},$$
(3)

is the total horizontal derivative of the magnetic field in the direction of x and y.

The analytical signal process is valuable in finding the boundaries of the magnetic field [63]. The benefit of utilizing the As-technique is to decide magnetic constraints from magnetic abnormalities. These include the freedom of magnetization inclination, less delicate noise in the data and interfering impact among shallow sources. Similarly, this change was regularly valuable at low magnetic latitudes, e.g., the investigated part [64]. Figure 7 reveals the As-map of the aeromagnetic data. This map designates that the high-values (AS-H) were detected at the northern, northwestern, northeastern, which indicated that these regions have significant magnetic contrasts that produce recognizable signatures (red colors) and few peak-values at the south and southeastern sides of the investigated area. The lineaments patterns resulting from this map are in the NE–SW, N–S, NW–SE, N–S, and E–W trends. Also, lower esteems of the As tendencies in the NE–SW and NW–SE are detected at numerous positions in the northern and south-central portions of the examined region.

Fig. 7
figure 7

The 3D analytical signal (As) map of Umm Tineidba area, Southern Eastern Desert, Egypt

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4.4 Tilt angle (Tg)

Miller and Singh [65] anticipated the tile-angle (Tg) as:

$$Tg={\mathit{tan}}^{-1}\left(\frac{-VDR}{THDR}\right).$$
(4)

The tilt angle (Tg) values have the property of presence ( +) over a magnetized source, fleeting during zero at the verge of a vertical-sided cause, and (–) esteem somewhere else (Miller and Singh 1994). A vital feature of the Tg is that the amplitudes of robust and frail anomalies can be adjusted adequately, enabling anomalies to be sketched out along-strike while generally ignoring the depth of the source [55, 65, 66]. Because of this, the Tg has an identical characteristic for various depth source and is capable of coming across the limits of the shallower and deeper sources. Verduzco et al. [63] have shown that the Tg-values are confined to values among + π/2 and − π/2 (+ 90° and − 90°) due to the natural property of the inverse tangent function. This information makes computing the Tg comparable to an automatic gain control filter. Also, the delineation of the depth to the vertical contact can be estimated from the half-distance between + π/4 and − π/4 [66].

Figure 8 illustrates that the projection of the magnetic field source focuses on the ground, is the fundamental dissemination in the Precambrian rocks, and also reveals that the zero relief path is sited near the fault interaction. The interpretation of the Tg map, applied on the RTP-map, outlines the changes anomalies between positive (orange and red colors) and negative values (yellow to blue colors), which demonstrate the alignment of anomalies. The Tg-map produces fully elongated zones and takes the NE–SW, NNE–SSW, NE–SW, and N–S trend directions.

Fig. 8
figure 8

The tilt angle (Tg) map applied on the RTP-map of Umm Tineidba area, Southern Eastern Desert, Egypt

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4.5 Local Wavenumber (LW)

The LW arises from the source parameter imaging technique [67], which evaluated the depth from the LW of the analytic signal. The K(x, y) gives the precise amount of modification of the local phase of the total-field of the horizontal (x and y) directions and simplified as:

$$K\left(x, y\right)=\frac{\frac{{\partial }^{2}T}{\partial x\partial z}{T}_{x}+\frac{{\partial }^{2}T}{\partial y\partial z}{T}_{y}+\frac{{\partial }^{2}T}{{\partial }^{2}z}{T}_{z}}{{\left(As\right)}^{2}},$$
(5)

where Tx, Ty, and Tz are the byproducts in x, y, and z-directions of the total-field. For contact, the maximum values of K are placed straight above the contact edges and liberated on the magnetic inclination, declination, dip, direction, and any vestige of magnetization. The interference is reduced due to using the 2nd-order imitative of the magnetic arena. The depth is appraised at the source edges from the following equation:

$$Depth= \frac{1}{{K}_{max}},$$
(6)

where Kmax is the extreme value of the LW and above the edge source.

Figure 9 shows the depth evaluation using the LW technique and demonstrates the depth ranges for the shallow structure is extended up to 350 m and for deeper structure lie between 400 and 1200 m.

Fig. 9
figure 9

The depth estimates using the local wave number (LW) technique of Umm Tineidba area, Southern Eastern Desert, Egypt

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5 Spectrometric Data Application

The gamma-ray spectroscopy data analysis purposes to localize anomalies, which include the uranium ores that could be correlated with lithology units and mineralization. However, the radiometric technique is best effective in regions controlled by the progressed intrusion, where the radioactive component deliberations are usually greater and revealed in a wide-range of various geologic settings. For example, massive sulfide and gold ores are commonly in the form of sericite [30].

Figure 10 demonstrated the whole amount of the gamma radiation (Tc in μR/h)) that point to three zones (differentiated by three different colors) founded in the examined region. The first one (Z1) in the middle of the area under investigation (Quaternary deposits and ophiolitic basic metavolcanic) trends N–S has a low radiometric concentration (≤ 4 μR/h). The second zone (Z2) is the intermediate region (4 to 7 μR/h) and mainly recorded over pre-Neoproterozoic or disinterred Neoproterozoic rocks and covered more than 50% of the study region. Finally, the third zone (Z3) (≥ 7 μR/h) is recorded over the granitic and metamorphosed rocks at the eastern part from N–S and in the NW part.

Fig. 10
figure 10

The total-count (Tc) of the Umm Tineidba area, Southern Eastern Desert, Egypt

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Furthermore, Fig. 11 demonstrates the elucidated point anomaly map of the area under investigation, which possesses values exceeding X + 2S for eU, eU/eTh, and eU/K variables. Various anomalous points were distinguished on this map [48]. The aero-radio-spectrometric maps show a wide record at different levels of rock protrusions and are controlled by the geological history of the examined area. Transitory explanations of the qualitative interpretation of the identified aero-radio-spectrometric maps with the characteristic rock suites are shown in Table 1.

Fig. 11
figure 11

Point anomaly map of the Umm Tineidba area, Southern Eastern Desert, Egypt [48]

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Table 1 Qualitative radio-spectrometric explanation for the main geologic units in the study area
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6 Results and Discussions

The trends of the interpreted features resulted from the residual and provincial maps are incorporated with the results from As and Tg methods (Fig. 12). Moreover, using airborne gamma ray spectrometric and different magnetic elucidation methods (As, Tg, for the RTP-map) help to determine the different locations of the main anomalies. So, the analysis of aeromagnetic lineaments from the residual and regional magnetic maps revealed the dominant trends include NE–SW and NNE–SSW and the subordinate ones comprise the N–S and E–W guidelines (Fig. 12) The dominant NE–SW trends were detected by Abdel Hafeez [48] and Essa [30] in their studies. The NE–SW trend is associated with the shear zones crossing the Pan-African belt, whereas the E–W patters are the products of the pre-Pan-African belt. The basement depths of magnetic sources from the RTP-magnetic map using the PS and the LW techniques are shown on the area (Table 2). Table 2 reveals that the depth of shallow structures extended up to 400 m and the depth of the deeper structure is also extended up to 1750 m. In addition, the increased percent of U-values in the Quaternary sediments places refer to leaks and migration from the granite to the wadis. This phenomenon is due to the migration and ascending of the deep hydrothermal fluids along the fault zones.

Fig. 12
figure 12

Interpreted structures and mineralized zones of the Umm Tineidba area, Southern Eastern Desert, Egypt

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Table 2 The interpreted results for the investigation area using the power spectrum (PS) technique and the local wavenumber (LW) technique
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6.1 Joint Interpretation of Available Data to Delineate Mineralized Zones

The magnetic and γ-spectrometric data display that the investigated region is exaggerated by severe tectonic deformations. The metagabbro and metadiorite rocks are categorized by numerous high magnetic anomalies, especially in the central part of the investigated area. The sheared hydrothermal deposits involving uranium, gold, and sulfide mineralization were intensively rehabilitated and by the later faults-controlled magmatic activity. These ore deposits show high magnetic anomalies near their boundaries and close to the younger granite and gneisses/migmatites along the structural lineaments and faulted zones (Fig. 12). The Umm Tineidba area and its environs show that their ore deposits have significant regional magnetic highs, which reflect that the durable magmatic activity could deliver respectable sources for the formation of diverse metallogenic systems. The latter are controlled by the NE and NW trending structures and their deep hydrothermal fluids deliver a good indication for gold mineralization. Therefore, the NE- and NW-trending shear zones were the main controlling structures, which facilitate the mineralizing magmatic ascent in the study area.

7 Conclusions

The objectives of this study included applying the available aeromagnetic and aero-spectrometric data for delineating and locating the sources that contain minerals deposits involving uranium, gold, and sulfide and the trend of the control lineament structures in the Gebel Umm Tineidba and its surroundings, Egypt. The total intensity (Tm) map, total count (Tc) map, and geological information of the study area were delineated. Ophiolitic mélanges sequences (serpentinites, gabbros, basic pillow volcanic) were delineated by a high magnetized source that is highly enriched in radioactive minerals (uranium, gold, and sulfide deposits) located by the Tm- and the RTP-maps. After a careful elucidation applying the power spectrum (PS), analytic signal (As), tilt angle (Tg), and local wavenumber (LW) methods, the study area has a multifaceted design of long and short wavelengths forming magnetic signatures that are inherited in Precambrian basement rocks. The pattern of total-intensity magnetic map reflects that the ore deposits are localized along the dominant trend of NE–SW and N–S with minor E–W and NW–SE lineament structures. The N–S, NE–SW, and NW–SE linear structures are related to Pan-African orogeny, whereas the E–W trend is to pre-Pan-African orogeny. Depth evaluations from PS and LW techniques publicized a dual layer deep and shallow (from 1750 to 400 m) depth source. The expected area for mineral and ores zones (Fig. 12) should be further studied to ensure our results.