Organic and Isotopic Geochemistry of Evaporites and Shales of the Santana Group (Araripe Basin, Brazil): Clues on the Evolution of Depositional Systems and Global Correlation during the Lower Cretaceous

: Even being the more studied of the interior basins of Northeast Brazil, the Araripe Basin still lacks research in organic geochemistry designed to support interpretations of depositional systems and conditions of formation. This work aims to investigate the organic behavior of evaporites and shales from the Santana Group (Lower Cretaceous), as well as discuss their role in the evolution of its depositional systems. A total of 23 samples, 17 shales and six evaporites, were collected in outcrops and quarries. Analyses of Total Organic Carbon (TOC), Total Sulfur (TS), Rock Eval pyrolysis, and the δ 34 S isotope ratio were performed. The TOC results revealed high organic content for seven intervals, of which only ﬁve had high TS content. From the Rock Eval pyrolysis, dominance of the Type I kerogen was veriﬁed, thus corresponding to the best type of organic matter (mainly algal) for the generation of liquid and gaseous hydrocarbons. The Lower Cretaceous (probably Aptian) response to the progressive evolution in redox conditions is linked to a remarked Oceanic Anoxic Event (OAE-1a). The TOC/TS ratio suggests variable palaeosalinity, indicating most of the shales were formed under brackish waters with saline inﬂuence, yet tending to increase the salinity upwards where hypersaline conditions dominate in the Ipubi Formation. The isotope data also suggest the occurrence of marine ingressions in the depositional systems even prior to the well-documented event of the Romualdo Formation. in seawater indicates that the mineralogy is a good proxy for the depositional conditions of the brines [90,91]. The δ 34 S V-CDT values of the gypsum from the studied samples are in agree with the normative values recorded by Claypool et al. (1980) [90] for Cretaceous evaporites (+13‰ to +20‰) interpreted as marine, then suggesting a marine water inﬂuence in the evaporites of the Ipubi Fm. based on its isotopic signature (Figure 8). For the modern ocean, the isotopic value of δ 34 S is between +20‰ and +21‰ [91,92].


Introduction
In ancient sedimentary basins, evaporites can record climatic, physiographic, environmental, and hydrochemistry changes. In this regard, some studies debate the marine or nonmarine origin for these sedimentary deposits (e.g., [1][2][3][4][5]). However, some evaporites show evidence of having formed from a mixture of open-ocean water and waters that record a continental influence (cf. [6]). In such a transitional environment, evaporites may

Geological Setting
The Araripe Basin (Figure 1), located in northeastern Brazil, was generated from tec-tonic events associated with the break-up of the West Gondwana paleocontinent and the opening of the modern Southern and Equatorial Atlantic Ocean [43]. The structural framework of the basin is linked to the reactivation of Precambrian basement structures, posteriorly favoring the opening of intracontinental rifts aborted from the Brazilian Northeast Rift System [44][45][46]. A transitional phase, amid the rift and the early post-rift (post-rift I) phases in the Araripe Basin, encompass the Barbalha, Crato, Ipubi, and Romualdo formations that compound the Santana Group [36]. These formations show a complex tectonic-sedimentary evolution formed by the stacking of several stratigraphic sequences limited by unconformities of regional nature [36,47]. Besides that, this succession also involves an interval recording a complete transgressive-regressive cycle, limited at the base by a pre-Aptian unconformity [46,48].
Minerals 2021, 11, x 3 of 22 mations that compound the Santana Group [36]. These formations show a complex tectonic-sedimentary evolution formed by the stacking of several stratigraphic sequences limited by unconformities of regional nature [36,47]. Besides that, this succession also involves an interval recording a complete transgressive-regressive cycle, limited at the base by a pre-Aptian unconformity [46,48]. The Santana Group, according to lithostratigraphic nomenclature propositions from Neumann and Cabrera (2002) [49], Assine et al. (2014) [36], and Neumann and Assine (2015) [47], involve laminated limestones, gypsum evaporites, sandstones, carbonate concretions, mudstones, siltstones, pelites, and dark shales [36,50]. At the base of this group, the Barbalha Formation occurs intercalating sandstones and shales, but also including black shales of the Batateira Bed, a highlighted stratigraphic marker that Hashimoto et al. (1987) [51] initially proposed as an organic-rich immature source rock. Overlying the Barbalha Formation are the Crato Formation, a unit which has an approximate thickness of 70 m [48]. This formation is composed predominantly of limestones with planar and parallel laminations containing widespread Dastilbe crandalli fish fossils [52][53][54], but also alternating shales between the limestone intervals. Some specific intervals inside the limestones are rich in famous, diverse, and exceptionally well-preserved fossils (i.e., [55]). Recent studies carried out on the Craton Formation have proposed a microbial nature for its limestones [56,57].
Discontinuous evaporite beds of the Ipubi Formation are deposited right above the Crato Formation and consist of gypsum-rich successions, interpreted as associated with coastal sabkhas [48] or a playa lake system [58]. Lastly, the Romualdo Formation is the uppermost lithostratigraphic unit of the Santana Gr. being mainly composed of shales, which is also recognized worldwide by its superb preservation of fossils inside carbonate concretions present in some levels (e.g., [59][60][61][62]). In a recent work, Custódio  The Santana Group, according to lithostratigraphic nomenclature propositions from Neumann and Cabrera (2002) [49], Assine et al. (2014) [36], and Neumann and Assine (2015) [47], involve laminated limestones, gypsum evaporites, sandstones, carbonate concretions, mudstones, siltstones, pelites, and dark shales [36,50]. At the base of this group, the Barbalha Formation occurs intercalating sandstones and shales, but also including black shales of the Batateira Bed, a highlighted stratigraphic marker that Hashimoto et al. (1987) [51] initially proposed as an organic-rich immature source rock. Overlying the Barbalha Formation are the Crato Formation, a unit which has an approximate thickness of 70 m [48]. This formation is composed predominantly of limestones with planar and parallel laminations containing widespread Dastilbe crandalli fish fossils [52][53][54], but also alternating shales between the limestone intervals. Some specific intervals inside the limestones are rich in famous, diverse, and exceptionally well-preserved fossils (i.e., [55]). Recent studies carried out on the Craton Formation have proposed a microbial nature for its limestones [56,57].
Discontinuous evaporite beds of the Ipubi Formation are deposited right above the Crato Formation and consist of gypsum-rich successions, interpreted as associated with coastal sabkhas [48] or a playa lake system [58]. Lastly, the Romualdo Formation is the uppermost lithostratigraphic unit of the Santana Gr. being mainly composed of shales, which is also recognized worldwide by its superb preservation of fossils inside carbonate concretions present in some levels (e.g., [59][60][61][62]). In a recent work, Custódio et al. (2017) [63] described a transgressive-regressive cycle in the Romualdo Formation in which the fossilbearing black shale would mark a maximum flooding surface. As a whole, the Santana Group is bounded by an unconformity at its top with the alluvial Araripina and Exu formations [36].

Samples
A total of six evaporite samples and 17 shale samples from the Santana Group were analyzed and interpreted in this study. The lateral correlation of the samples was made through six columnar sections, exhibiting the stratigraphic position of the rocks ( Figure 2). The samples were collected along stratigraphic sections denominated Batateira River (BTRS), Sobradinho River (SBRS), Rancharia Mine (RCMS), São Jorge Mine (SJMS), Gesso Chaves Mine (GCMS), and Conceição Preta Mine (CPMS) (Figures 1 and 2). The shale samples are dominated by dark green, gray, and black lithics, whereas evaporite samples were mainly white luster, massive gypsum layers (Figures 2 and 3); both rocks were directly selected from outcrops and quarries in the sections. The samples belong to the same collecting sites of the work from Chagas (2017) [64,65], who collect them originally for facies and palynologic purposes.
Minerals 2021, 11, x 4 of 22 [63] described a transgressive-regressive cycle in the Romualdo Formation in which the fossil-bearing black shale would mark a maximum flooding surface. As a whole, the Santana Group is bounded by an unconformity at its top with the alluvial Araripina and Exu formations [36].

Samples
A total of six evaporite samples and 17 shale samples from the Santana Group were analyzed and interpreted in this study. The lateral correlation of the samples was made through six columnar sections, exhibiting the stratigraphic position of the rocks ( Figure  2). The samples were collected along stratigraphic sections denominated Batateira River (BTRS), Sobradinho River (SBRS), Rancharia Mine (RCMS), São Jorge Mine (SJMS), Gesso Chaves Mine (GCMS), and Conceição Preta Mine (CPMS) (Figures 1 and 2). The shale samples are dominated by dark green, gray, and black lithics, whereas evaporite samples were mainly white luster, massive gypsum layers (Figures 2 and 3); both rocks were directly selected from outcrops and quarries in the sections. The samples belong to the same collecting sites of the work from Chagas (2017) [64,65], who collect them originally for facies and palynologic purposes.   The dataset obtained from the shale samples include total organic carbon content (TOC), total sulfur content (TS), Rock-Eval Pyrolysis index (RE), and isotopic ratios of sulfur (δ 34 SV-CDT). For the evaporite samples, only the isotopic analysis of sulfur was performed. All analyses were made at the Geochemistry Laboratory of the Leopoldo Américo Miguez de Mello Research and Development Center (CENPES) of Petrobras.  The dataset obtained from the shale samples include total organic carbon content (TOC), total sulfur content (TS), Rock-Eval Pyrolysis index (RE), and isotopic ratios of sulfur (δ 34 S V-CDT ). For the evaporite samples, only the isotopic analysis of sulfur was performed. All analyses were made at the Geochemistry Laboratory of the Leopoldo Américo Miguez de Mello Research and Development Center (CENPES) of Petrobras.

TOC and TS
The determination of total sulfur contents in rocks by itself does not provide detailed information, being generally evaluated in conjunction with TOC data, thus providing valuable subsidies to the interpretation of the depositional environment in which the rock was formed [66], and can be interpreted in terms of paleosalinity of the depositional system.
Initially, an aliquot of 250 g of each shale sample was crushed and then sieved with an 80-mesh sieve. Then, the powdered samples were reacted with 32% hydrochloric acid to eliminate eventual inorganic carbon from carbonates. After this, the samples were washed with distilled water to remove traces of HCl. The samples were also dried in an oven at 60 • C and, after cooling, total organic carbon and sulfur were measured. The reliability of all the selected samples were tested before measuring the carbon-sulfur analyses using a LECO-SC144DR device.

Rock-Eval Pyrolysis
For the analysis of the source rock potential through pyrolysis, samples that yielded TOC contents lower than one weight percent (1 wt%) were discarded, following the recommendation of [67]. Only seven samples provided TOC values higher than 1% and thus have pyrolysis analyses. The four parameters obtained from the pyrolysis were: The amount of free hydrocarbons present within the sample (S1 curve, mg HC/g rock), hydrocarbons generated from the cracking of kerogen (S 2 curve, mg HC/g rock), Tmax (thermal maturity proxy, calculated from the temperature peak of the S 2 curve, in • C), and carbon dioxide (CO 2 ) released during the analyses (S 3 values, CO 2 /g rock). These parameters followed the method described by Espitalié et al. (1977) [68]. During analysis, the samples were heated under an inert atmosphere of helium. This technique was performed in a flame ionization detector sensitive to organic compounds emitted during three heating steps, while sensitive infrared detectors measured CO and CO 2 during pyrolysis and oxidation [69].
Additionally, two other derived parameters were calculated: The hydrogen index (HI) or hydrogen to carbon ratio (H/C), that is equal to (S 2 /TOC) × 100, and the oxygen index (O/I) or oxygen to carbon ratio (O/C), that is equal to (S 3 /TOC) × 100 [70]. The HI and OI furnish an estimation of the organic matter type by indicating the type of kerogen present within the sample, being posteriorly plotted on a Van Krevelen diagram. A classic differentiation of the type of organic matter (kerogen types I, II, and III) follows the proposal by Tissot and Welte (1978) [71].

Sulfur Isotope Analysis
Among the 17 initial samples of shale, six presented less than 0.01% of total sulfur, which is insufficient for sulfur isotopic analysis. For the remaining 11 shale samples, as well as for the six evaporite samples, the sulfur isotopic ratios ( 34 S/ 32 S) were measured in a Finnigan Mat 252 mass spectrometer. The sulfur isotopic values here are reported in δ 34 S in parts per mill (‰) of deviation relative to the established Vienna Canyon Diablo troilite standard (V-CDT) (IAEA standard S-1). The analytical precision of the method is ±0.2‰ for δ 34 S.

Results and Interpretations
Rock-Eval parameters (HI and OI), total organic carbon (TOC), sulfur content (TS), and the bulk organic sulfur isotopic composition (δ 34 S) of a sample give valuable clues on the type of kerogen, the maturity of the organic matter present, the salinity, and oxygenation.  Table 1 exhibits the analytical results of geochemical and isotopic analysis of them. Table 1. Total sulfur (TS), total organic carbon (TOC), hydrogen index (HI), oxygen index (OI), and sulfur isotopic (δ 34 S) values obtained for the investigated lithotypes. The vertical stacking is in agree with the stratigraphic positioning of the collected samples.

Chemostratigraphic Units
Five chemostratigraphic units, named A to E, were defined for the studied interval from the TOC, insoluble residue (IR), and TS geochemical data, as shown in Figure 4. In the following section, Figure 4 presents a detailed description.

Unit A
The lowermost chemostratigraphic unit ( Figure 4) includes the lower half of the Barbalha Fm., from its ordinary basal gray shales to the black shales of the Batateira Bed. This interval is equivalent to the so-called "first fluvial cycle"-i.e., Assine 2007 [48], believed to encompass riverine braided systems gradually replaced by a lacustrine establishment at the top. The unit A is characterized by TOC values ranging from 0.4% to 13.7%, total sulfur from 0.04 to 0.11, and insoluble residue (IR) from 31% to 89%. All terrigenous shale samples presented insoluble residue values above 70%, while lower values were found in calcitic shales. In particular, the Batateira Bed shows a high content of total organic carbon (13.7%), total sulfur of 1.3%, and insoluble residue of only 31%, the lowest among all samples.

Unit B
The second unit is highlighted by low values of TOC (between 0.34% and 0.72%) and total sulfur (0.01%) ( Figure 4). The presence of carbonates in the insoluble residue is noted only in the sample DR-BA-22 (calcitic shale), as characterized in the section studied by Chagas (2017) [65], where there is a gradual transition from black shales to finely laminated gray to cream colored limestones from the Crato Formation. Minerals 2021, 11, x 8 of 22

Unit A
The lowermost chemostratigraphic unit ( Figure 4) includes the lower half of the Barbalha Fm., from its ordinary basal gray shales to the black shales of the Batateira Bed. This interval is equivalent to the so-called "first fluvial cycle"-i.e., Assine 2007 [48], believed to encompass riverine braided systems gradually replaced by a lacustrine establishment at the top. The unit A is characterized by TOC values ranging from 0.4% to 13.7%, total sulfur from 0.04 to 0.11, and insoluble residue (IR) from 31% to 89%. All terrigenous shale samples presented insoluble residue values above 70%, while lower values were found in calcitic shales. In particular, the Batateira Bed shows a high content of total organic carbon (13.7%), total sulfur of 1.3%, and insoluble residue of only 31%, the lowest among all samples.

Unit B
The second unit is highlighted by low values of TOC (between 0.34% and 0.72%) and total sulfur (0.01%) (Figure 4). The presence of carbonates in the insoluble residue is noted only in the sample DR-BA-22 (calcitic shale), as characterized in the section studied by Chagas (2017) [65], where there is a gradual transition from black shales to finely laminated gray to cream colored limestones from the Crato Formation.

Unit E
The topmost unit starts with almost zero total sulfur values at the base, then progressively increases towards the top (Figure 4). At the same time, TOC ranges from 0.09% to 1.04% at the base and with a significant increase to the top. The samples at the top are DR-BA-20 (3.92% TOC and 0.97% total sulfur) and DR-BA-19 (5.65% TOC and 1.25% total sulfur), being shales of the Romualdo Fm.

Relationship between Total Organic Carbon and Total Sulfur
The TOC of the analyzed shales presented values between 0.01% and 23.3%, while the sulfur values ranged from 0.01% to 3.41% (Table 1). Based on analyses of numerous samples from ancient and recent depositional systems, Berner and Raiswell (1983) [72] and Leventhal (1995) [73] concluded the existence of a good linear correlation between organic carbon and sulfur (in the form of sulfide) contents in fine sediments, from which it would be possible to discriminate the paleosalinity of waters of the depositional systems into hypersaline, saline, and fresh. According to Raiswell (1984) [74], under anoxic conditions, bacteria promote the reduction of sulfates, having H 2 S as one of the products; if detrital iron is available, it reacts to H 2 S, then generating sedimentary pyrite. In the case of seawater, this contains a larger amount of dissolved sulfates, and therefore, in a marine environment, the formation of sedimentary pyrite would be greater than in freshwater environments. This interpretation, however, requires great caution because it compares marine depositional systems in terms of salinity, whose relationship is not always straightforward in continental systems (i.e., oxygenated, endorheic/evaporitic lakes).
Paleosalinity variations are also interpreted by Woolfe et al. (1995) [75], based on the calculation of the C/S ratio, where they synthesized the method so that the parameters also apply to oxygenated waters: 1.5-4.0 (normal marine salinity); 4.0-11.0 (brackish with saline influence); 11.0-17.0 (brackish with freshwater influence); more than 17.0 (freshwater environment). In combination with the total organic carbon content of this research, the total sulfur content was deposited partly under anoxic conditions, whose C/S ratio is classified in Figure 5.  Leventhal, 1995 [73]) and the C/S ratio (after Woolfe et al. 1995 [75]) to interpret paleosalinity of the Santana Group.
Usually, low TOC values indicate that little or no organic matter is being preserved and suggest oxic conditions [66]. In the other hand, different sub-environments in the depositional systems can develop dominantly anoxic conditions when the input rate of degradable organic matter exceeds oxygen diffusion, so the oxygen can be depleted at the water-sediment interface of water bodies with restricted circulation. Significant anoxic events such as OAE's (Oceanic Anoxic Events) consist of global episodes favoring organic carbon deposition and preservation [76] as a response on oceanic variations, i.e., reduced  Leventhal, 1995 [73]) and the C/S ratio (after Woolfe et al. 1995 [75]) to interpret paleosalinity of the Santana Group.
Usually, low TOC values indicate that little or no organic matter is being preserved and suggest oxic conditions [66]. In the other hand, different sub-environments in the depositional systems can develop dominantly anoxic conditions when the input rate of degradable organic matter exceeds oxygen diffusion, so the oxygen can be depleted at the water-sediment interface of water bodies with restricted circulation. Significant anoxic events such as OAE's (Oceanic Anoxic Events) consist of global episodes favoring organic carbon deposition and preservation [76] as a response on oceanic variations, i.e., reduced oxygenation level, sea-level rise, etc. Several models suggest even episodic causes for these events, such as restriction of paleogeographic environments relative to the oceans, stagnation of oceanic currents, increased continental surface runoff, abnormally high organic productivity, and intense and widespread deep-sea volcanic activity [77]. In the continental domain, anoxic conditions are more geographically restricted and may occur in lacustrine systems or those bearing flooded soils [78], such as floodplains of riverine systems.
The Barbalha Fm. is traditionally interpreted as being formed by two fluvial cycles finalized by dominantly lacustrine systems, the first of which ended in the Batateira Bed [48]. In this work, one sample from the first fluvial cycle falls within the field interpreted as brackish with freshwater influence, suggesting that arid conditions early began to reach the fluvial system of Barbalha Fm.; however, the overlying samples (including the Batateira Bed) fall into the brackish conditions with saline influence. For the Batateira Bed, the TOC and TS values are high (13.7% and 1.3%, respectively), suggesting an origin possibly related to a moment of maximum flooding, whose base level elevation would have contributed to anoxia in the system. There, a mild increase in the salinity could come from more arid conditions and/or invasion by marine waters.
In the Crato Fm., which is to date interpreted as a lacustrine system due to its fossiliferous association in the laminated limestones and an apparent absence of marine clues [48], the samples of shale fall within the context of a freshwater environment, with low TOC (<0.72%) and total sulfur (<0.1%) contents. Shales and limestones are the main rocks occurring interdigitated in the Crato Fm., whose paleogeography is thought to be a fragmented lacustrine system for most of the unit's history, rather than a single large lake, as the shales are formed under relatively shallower water than the limestones, and are also more abundant towards the basin boundaries [47,49]. There is evidence of aridity reached in the limestone layers, such as halite pseudomorphs [41]; however, the vertical stacking of limestones passing to shales demonstrate that moments of lacustrine spatial restriction occurred. Since the interlayered shales were precisely the rocks sampled in the present study, there is still a chance that the climate was possibly wetter in these intervals. In this case, one possibility for the result of the present study would be the presence of fresher and shallower lake waters, which in the latter respect would still facilitate circulation under more oxidizing conditions at the bottom.
In the Ipubi Fm, the shales occur with results indicating normal marine salinity and brackish salinity with marine influence, matching similar conditions of the evaporites in the same unit. In lakes, the variation in salinity is generally related to their depth: The deeper and more stratified the lake, the higher the salt concentration in the hypolimnion [79]. Water salinity also intensely influences the abundance and variety of organisms in lake ecosystems, decreasing the primary productivity as the salinity increases [80]. However, extremely-high salinity (hypersalinity) invariably relates to high temperature due to more intense evaporation [81] and a higher saturation of salts in a relatively smaller aqueous volume. Samples collected at Nova Olinda (north of the basin) suggest more saline conditions than those collected at Araripina and Trindade (south of the basin), suggesting more significant restriction and/or effective evaporation from endorheic waters in the northern portions.
Finally, at Romualdo Fm., the samples suggest sedimentation in conditions with C/S ratios strongly variable, from low to high values, i.e., with abrupt salinity increment, which may have facilitated the mortality of freshwater fishes recorded exactly at the place where fossiliferous carbonate concretions (ichthyolites) are found [82,83]. Notwithstanding, the association of carbonate-pelitic lithofacies of the Romualdo Formation also preserved fossil fishes tolerant to high saline conditions, being in the deeper strata the mixed haline genus Calamopleurus [38], and in the more superficial ones some frankly marine genera like Rhacolepis and Vinctifer [84].

Organic Matter Type
The study of kerogen types positioned the analyzed samples dominantly between the fields of Types I and III of organic matter (Figure 6), then encompassing freshwater algal and marine or lacustrine planktonic origin but also humic organic matter, derived from terrestrial plants [68]. Samples with Type I kerogen (DR-BA-11, DR-BA-17, DR-BA-20, and DR-BA-15) would thus have the best type of organic matter for liquid and gaseous hydrocarbon generation. In contrast, samples with Types II and III kerogens (DR-BA-05, DR-BA-09, and DR-BA-19) would comprise samples with lower potential in hydrocarbon generation.   Table 1). The discriminant f following Espitalié et al. (1977) [68].

Sulfur Isotopic Clues
The results of the sulfur isotopic analysis (δ 34 SV-CDT) are shown in Table 1 and 7 where the samples of shale showed a variation from −16.36‰ to −5.27‰ and evaporite from +16.51‰ to +17.71‰.

Sulfur Isotopic Clues
The results of the sulfur isotopic analysis (δ 34 S V-CDT ) are shown in Table 1 and Figure 7 where the samples of shale showed a variation from −16.36‰ to −5.27‰ and those of evaporite from +16.51‰ to +17.71‰.  [36] assumed three MFSs inside the Santana Group based on the gamma-ray of well profiling that coincides with the MFSs of the present research. These flooding surfaces also match with the boundaries of the so-called "Depositional Sequence 1" (DS-1), "Depositional Sequence 2" (DS-2), and "Depositional Sequence 3" (DS-3) of that study [36]. The contact between DS-1 and DS-2 is positioned on the marly shales of the Batateira Bed, while the contact between DS-2 and DS-3 is positioned on the evaporitic section of the Ipubi Fm. Inside the DS-3, the flooding surface was positioned in the upper portion of a dominantly transgressive system tract succession, in this case, the shales with fossiliferous concretions at the level of bioclastic limestones of the Romualdo Fm.
The Batateira Bed showed an isotopic value of −13.35‰, a value typical of a lacustrine system; negative values like this indicate that much of the existing sulfur is of bacterial origin, favoring enrichment in the light isotope ( 32 S). Farina (1974) [85] named the Batateira Bed as a "plumbiferous sequence" due to a mineralization in lead, zinc, and copper sulfides that generally associate with an intermediate lens of limestone or marl inside the unit. Therefore, it is believed that hydrogen sulfide has been produced by bacterial reduction under anaerobic conditions. It may have been fixed in the sediment as pyrite and as organic sulfur. For Rios-Netto et al. (2012) [86], the combined lithological and palynological features, including the presence of Botryococcus algae, indicate deposition in a shallow lacustrine environment, also arguing that none marine palynomorphs were found. The  [36] assumed three MFSs inside the Santana Group based on the gamma-ray of well profiling that coincides with the MFSs of the present research. These flooding surfaces also match with the boundaries of the so-called "Depositional Sequence 1" (DS-1), "Depositional Sequence 2" (DS-2), and "Depositional Sequence 3" (DS-3) of that study [36]. The contact between DS-1 and DS-2 is positioned on the marly shales of the Batateira Bed, while the contact between DS-2 and DS-3 is positioned on the evaporitic section of the Ipubi Fm. Inside the DS-3, the flooding surface was positioned in the upper portion of a dominantly transgressive system tract succession, in this case, the shales with fossiliferous concretions at the level of bioclastic limestones of the Romualdo Fm.
The Batateira Bed showed an isotopic value of −13.35‰, a value typical of a lacustrine system; negative values like this indicate that much of the existing sulfur is of bacterial origin, favoring enrichment in the light isotope ( 32 S). Farina (1974) [85] named the Batateira Bed as a "plumbiferous sequence" due to a mineralization in lead, zinc, and copper sulfides that generally associate with an intermediate lens of limestone or marl inside the unit. Therefore, it is believed that hydrogen sulfide has been produced by bacterial reduction under anaerobic conditions. It may have been fixed in the sediment as pyrite and as organic sulfur. For Rios-Netto et al. (2012) [86], the combined lithological and palynological features, including the presence of Botryococcus algae, indicate deposition in a shallow lacustrine environment, also arguing that none marine palynomorphs were found. The shale immediately below the Batateira Bed resulted in a δ 34 S V-CDT of −5.27‰; in this case, one possibility is that the environment was more oxygenated and with a decreasing influence of anaerobic bacterial activity. In the Crato Fm., the samples obtained low total sulfur results (0.01%), making δ 34 S V-CDT isotopic analysis impossible for the used method.
There is no consensus on the depositional system for the origin of the evaporites of Ipubi Fm. In his early research, Lima (1978) [87], based on micropaleontological association, positioned the formation in a transitional environment, arguing that there is no evidence for the existence of a broad marine basin nor an exclusively continental system. For its turn, Arai and Coimbra (1990) [88] detected the presence of a fossiliferous assembly composed of pollen, spores, dinoflagellates, ostracods, foraminifera, and mollusks typical of coastal environments with "unquestionable" marine influence. Soon after, Assine (1992) [89] interpreted the unit as formed in arid coastal systems of a supratidal realm (sabkha) exposed to sea-level variations. More recently, Nascimento et al. (2016) [58], based on facies, petrography, mineralogy, and chemical analyses, have hypothesized the possibility of a playa lake-like system subject to salinity oscillations and perhaps surface hydrothermalism, but with no marine connection.
Geochemically, sulfate is comparatively abundant in seawater, which is why the zone of sulfur-reducing bacteria is extensive, and the sulfate concentration in lakes is lower [78]. The isotopic results for all evaporite samples in this study indicated enrichment in the heavy isotope ( 34 S, with δ 34 S V-CDT values of +16.51‰ to +17.71‰), and a value of approximately 1‰ higher was noticeable in samples of the Ipubi Fm. collected southwards in the Pernambuco State when compared to those collected in Ceará (this work), demonstrating that sulfate reduction was higher in the latter region. It is known that the similarity between δ 34 S values of sulfate minerals and dissolved sulfate in seawater indicates that the mineralogy is a good proxy for the depositional conditions of the brines [90,91]. The δ 34 S V-CDT values of the gypsum from the studied samples are in agree with the normative values recorded by Claypool et al. (1980) [90] for Cretaceous evaporites (+13‰ to +20‰) interpreted as marine, then suggesting a marine water influence in the evaporites of the Ipubi Fm. based on its isotopic signature (Figure 8). For the modern ocean, the isotopic value of δ 34 S is between +20‰ and +21‰ [91,92]. ence of anaerobic bacterial activity. In the Crato Fm., the samples obtained low total sulfur results (0.01%), making δ 34 SV-CDT isotopic analysis impossible for the used method.
There is no consensus on the depositional system for the origin of the evaporites of Ipubi Fm. In his early research, Lima (1978) [87], based on micropaleontological association, positioned the formation in a transitional environment, arguing that there is no evidence for the existence of a broad marine basin nor an exclusively continental system. For its turn, Arai and Coimbra (1990) [88] detected the presence of a fossiliferous assembly composed of pollen, spores, dinoflagellates, ostracods, foraminifera, and mollusks typical of coastal environments with "unquestionable" marine influence. Soon after, Assine (1992) [89] interpreted the unit as formed in arid coastal systems of a supratidal realm (sabkha) exposed to sea-level variations. More recently, Nascimento et al. (2016) [58], based on facies, petrography, mineralogy, and chemical analyses, have hypothesized the possibility of a playa lake-like system subject to salinity oscillations and perhaps surface hydrothermalism, but with no marine connection.
Geochemically, sulfate is comparatively abundant in seawater, which is why the zone of sulfur-reducing bacteria is extensive, and the sulfate concentration in lakes is lower [78]. The isotopic results for all evaporite samples in this study indicated enrichment in the heavy isotope ( 34 S, with δ 34 SV-CDT values of +16.51‰ to +17.71‰), and a value of approximately 1‰ higher was noticeable in samples of the Ipubi Fm. collected southwards in the Pernambuco State when compared to those collected in Ceará (this work), demonstrating that sulfate reduction was higher in the latter region. It is known that the similarity between δ 34 S values of sulfate minerals and dissolved sulfate in seawater indicates that the mineralogy is a good proxy for the depositional conditions of the brines [90,91]. The δ 34 SV-CDT values of the gypsum from the studied samples are in agree with the normative values recorded by Claypool et al. (1980) [90] for Cretaceous evaporites (+13‰ to +20‰) interpreted as marine, then suggesting a marine water influence in the evaporites of the Ipubi Fm. based on its isotopic signature (Figure 8). For the modern ocean, the isotopic value of δ 34 S is between +20‰ and +21‰ [91,92].  Claypool (1980) [90]. Data from North America, Central America, Brazil/Angola (only from the coastal basins), Mediterranean, Northern Europe, and this research.
The reduction of sulfate generates a kinetic effect on sulfur isotope fractioning, causing the hydrogen sulfide generated to be depleted in the heavy isotope 34 S [93]. For Bottrell and Newton (2006) [94], this happens due to the predilection of bacteria for the lighter Figure 8. Global curve of sulfur isotopic variations in marine evaporites from the Cretaceous modified from Claypool (1980) [90]. Data from North America, Central America, Brazil/Angola (only from the coastal basins), Mediterranean, Northern Europe, and this research.
The reduction of sulfate generates a kinetic effect on sulfur isotope fractioning, causing the hydrogen sulfide generated to be depleted in the heavy isotope 34 S [93]. For Bottrell and Newton (2006) [94], this happens due to the predilection of bacteria for the lighter isotope. Therefore, the composition of sedimentary sulfides would reflect the chemical, isotopic composition of hydrogen sulfide produced during sulfate reduction [95]. Studies by Fry et al. (1991) [96] and Neretin et al. (1998) [97] show that sulfides in sediments or waters under euxinic conditions are commonly depleted in 34 S with a range of −45‰ to −70‰ relative to seawater sulfate.
In the present study, the compared isotopic results of evaporites and shales of the Ipubi Fm. are contrasting, being enriched in 34 S in the first case and depleted in the second case. This situation indicates that this depletion of the heavy isotope in the shales is associated with the dissimilatory reduction of sulfate by bacteria that is balanced by the enrichment of 34 S in the water sulfate (generator of the evaporites). In periods of high biological activity by sulfate-reducing bacteria, there is an increase of the 34 S value in the waters (and their evaporites), especially in the oceans, due to the preferential removal of 34 S-depleted sulfur as sedimentary sulfides [91]. This would explain the significantly negative values for the shales situated at the base of the evaporites in contrast to the isotopic values of the evaporites themselves, thus suggesting an isotopic signature of marine composition. The isotopic values for the evaporites in this research are within the range of +10.27‰ to +17.99‰ found by Barros et al. (2016) [98] and Bobco et al. (2017) [26], where they interpreted evaporitic subaqueous systems with seawater mixing at times, and also a marine origin for the brine generating the evaporitic deposits, respectively.
In the Romualdo Formation, the δ 34 S isotopic results of the shales located just above the second (last) evaporite layer of the Ipubi Formation were −12.85‰ (DR-BA-04) and, soon above, −9.6‰ (DR-BA-05). Thus, there is a slight enrichment of the 34 S isotope even when compared to the shales from beneath the evaporites. This enrichment could be influenced by a mixing of waters (marine and lacustrine). It is known that several forms of dinoflagellates were recognized in the shales just above the gypsum of the Ipubi Formation [87]. Arai and Coimbra (1990) [88] also recognized dinoflagellates of the genera Subtilisphaera and Spiriferites, suggesting marine influence in their depositional environment. Importantly, Chagas (2017) [65] identified groups of marine palynomorphs (i.e., Rodonascia bontei) at the same stratigraphic levels of this research in both the base and top shales of the Ipubi Formation, ratifying marine ingressions, as well as a coincidence with levels with high percentages of the genus Classopollis, which are generally associated with deposits near coastal regions. In the case of the sample DR-BA-06, it was not possible to perform δ 34 S isotopic analysis because it had an insufficient amount of total sulfur (0.01%), in addition to possibly anoxic conditions (TOC of 0.11%) ( Figure 9). However, following towards the top of the Santana Group, two samples were collected in the interval bearing the fossiliferous carbonate concretions, where the isotopic results were −9.83‰ and −10.06‰, implying a slight enrichment in 34 S. In this same interval, Chagas (2017) [65] found the dinoflagellate Subtilisphaera senegalensis, also considered a marine indicator.
The redox conditions during the deposition of the Santana Group, obtained from the TOC and total sulfur geochemical data, provide constraints on the evolution of the Araripe Basin. These are consistent with previous paleontological and organic biomarker data that indicate saline and redox-stratified conditions in the depositional basin ( Figure 9). The Barbalha and Crato formations showed TOC/TS ratios suggesting deposition in a mainly freshwater lacustrine depositional environment, a result in agreement with most of the former research (i.e., [41,[102][103][104]). Usually, the sulfur isotopic data are also consistent with oxic conditions, a finding that also match recent work by   [105] who interpreted the Barbalha-Crato interval as deposited in a dominantly freshwater lacustrine system due to the abundance of non-marine fossils and an oxygen isotopic ratio (δ 18 O V-PDB ) between −6.9‰ and −4.48‰. The redox conditions during the deposition of the Santana Group, obtained from the TOC and total sulfur geochemical data, provide constraints on the evolution of the Araripe Basin. These are consistent with previous paleontological and organic biomarker data that indicate saline and redox-stratified conditions in the depositional basin ( Figure 9). The Barbalha and Crato formations showed TOC/TS ratios suggesting deposition in a mainly freshwater lacustrine depositional environment, a result in agreement with most of the former research (i.e., [41,[102][103][104]). Usually, the sulfur isotopic data are also consistent with oxic conditions, a finding that also match recent work by  [105] who interpreted the Barbalha-Crato interval as deposited in a dominantly freshwater lacustrine system due to the abundance of non-marine fossils and an oxygen isotopic ratio (δ 18 OV-PDB) between −6.9‰ and −4.48‰.
Particularly, the Ipubi Formation would represent a regional expansion of anoxic conditions, and most of the studied samples indicate anoxic or periodic anoxic conditions. Besides that, the salinity indicates the transition between brackish waters with saline influence to a water with normal sea salinity. The evaporitic succession is a piece of evidence that the Araripe Basin experienced severe climatic and salinity variations [26,41,57,106]. Recent works [27,107] also point that the evaporites of the Ipubi Formation may have putatively precipitated by the evaporation of marine waters. These findings, as in the present work, point for intermittent marine incursions in the Ipubi Formation [105] rather than an isolated playa-lake environment [58], in a probable true coastal sabkha system [48].
Finally, the Romualdo Formation presents strongly variable signatures of paleoredox conditions (Figure 9), being euxinic conditions with periodic anoxia occurring in samples related to the shale layers with fossiliferous concretions (DR-BA-19 and DR-BA-20), once more pointing to a cause for the mortality recorded in that interval (i.e., [48]), despite not explaining the origin for the (local?) anoxia. The salinity attests for waters under brackish conditions with marine influence ( Figure 5). Marine behavior for the Romualdo Formation Particularly, the Ipubi Formation would represent a regional expansion of anoxic conditions, and most of the studied samples indicate anoxic or periodic anoxic conditions. Besides that, the salinity indicates the transition between brackish waters with saline influence to a water with normal sea salinity. The evaporitic succession is a piece of evidence that the Araripe Basin experienced severe climatic and salinity variations [26,41,57,106]. Recent works [27,107] also point that the evaporites of the Ipubi Formation may have putatively precipitated by the evaporation of marine waters. These findings, as in the present work, point for intermittent marine incursions in the Ipubi Formation [105] rather than an isolated playa-lake environment [58], in a probable true coastal sabkha system [48].
Finally, the Romualdo Formation presents strongly variable signatures of paleoredox conditions (Figure 9), being euxinic conditions with periodic anoxia occurring in samples related to the shale layers with fossiliferous concretions (DR-BA-19 and DR-BA-20), once more pointing to a cause for the mortality recorded in that interval (i.e., [48]), despite not explaining the origin for the (local?) anoxia. The salinity attests for waters under brackish conditions with marine influence ( Figure 5). Marine behavior for the Romualdo Formation is well documented (i.e., [48,88]), but only recently have some works gathered evidence for a true epicontinental sea [105,108].

Global Correlation Based on the Oceanic Anoxic Events
In the Araripe Basin, the Santana Group are recently under debate regarding its chronological positioning inside the Lower Cretaceous [28,[109][110][111], where the traditional view on ages extending into the Albian (Aptian-Albian) is questioned. Despite being studied long ago with microfossils as a basis for correlation [37], the group is still scarce in reliable levels that would be directly correlated with other basins, thus influencing on the precision time-interval of the unit.
Globally well-known oceanic anoxic events (OAE) can be useful in track specific positions inside marine-influenced basins, therefore helping correlation efforts. Once marine flooding events are frequently associated with OAEs, any tools designed to detect this association are useful. In this sense, Assine et al. (2014) [36] recognized three MFSs in the Santana Group, based on gamma-ray data and facies analysis, where at least one global OAEs would be fit based in the time interval. The three MFSs were positioned: i. at the Batateira Bed (inside the Barbalha Fm.); ii. at the base of the Ipubi Fm.; and iii. at the beginning of the final third of the Romualdo Fm. Based on recent works assuming the Ipubi Fm. is deposited in the Late Barremian-Early Aptian interval (126.5-119.5 Ma; [110]) and the Romualdo Fm. as deposited prior the Late Aptian terminus (~113 Ma; [28]), the Selli Event (OEA-1a,~120 Ma; [112]) would be the only with chances of a record inside the Santana Gr., thus positioned inside the base of the Ipubi Fm. This is coincident with the position where two samples of shale presented the highest TOC and TS values (Table 1, Figure 9) among the overall samples of the Santana Gr.

Conclusions
The Santana Group presented, for the analyzed samples of evaporites and shales, high organic richness, with excellent averages of preserved organic matter in seven studied intervals. Three anoxic events would be associated with environmental changes in short time intervals and may correlate with maximum flooding surfaces (MFSs) located in the Barbalha (Batateira Bed), Ipubi, and Romualdo formations. The shales of the Barbalha Fm. showed congruence with freshwater (lacustrine/fluvial), except for the Batateira Bed, with a trend of slightly increased salinity, but still with Type I kerogen (lacustrine algal organic matter) and δ 34 S indicative of lacustrine system with significant bacterial activity. Shales from the Crato Formation showed low amounts of TS, making δ 34 S analyses impossible; however, their results suggest lacustrine systems in a dominantly freshwater environment. For its turn, Ipubi Formation presented characteristics of an environment rich in saline to hypersaline water, with Type I kerogen and sulfur isotopes relatively enriched in 32 S in the shales (due to a reducing bacterial activity) and 34 S in the adjacent evaporites, an association suggestive of marine influence. In the Romualdo Formation, half of the samples of shale presented affinity with saline to hypersaline water; moreover, kerogen oscillated between types I and II, and with sulfur isotopic values of −9.83‰ and −10.06‰, and thus may characterize the shales in a depositional system varying from eventually to dominantly-reached by marine water inputs.
The Selli Event (OAE-1a) is the probable global anoxic event recorded inside the Santana Gr., once Ipubi Fm. has clues of marine incursions and the probable age involved fits well. This interpretation reinforces recent publications that consider the entire Santana Gr. as deposited strictly before the Albian in the Lower Cretaceous. manuscript, and the editorial staff of the journal for the assistance along the submitting process. In particular, N.V.P. and D.B.d.C. acknowledge Fundação Cearense de Apoio ao Desenvolvimento Científico e Tecnológico (Funcap) for their doctorate fellowships.

Conflicts of Interest:
The authors declare no conflict of interest.