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Paratethys

Paratethys was a vast epicontinental sea system that occupied southeastern Europe and western Asia from the Eocene/Oligocene boundary (approximately 33.9 million years ago) until the Pleistocene, originating as a fragmented remnant of the ancient Tethys Ocean due to tectonic closure driven by the Alpine orogeny.^[1] It initially formed at the rear of the Tethys closure front, encompassing two primary basins: the Central Paratethys (Carpathian region) and the Eastern Paratethys (Euxine-Caspian area).^[2] Geographically, it extended from the Eastern Alps and North Alpine Foreland Basin in the west to the Aral Sea region in Central Asia, with southern boundaries defined by orogenic belts such as the Dinarides, Pontides, Lesser Caucasus, and Elburz Mountains.^[1]^[2] The Paratethys evolved through distinct phases influenced by tectonic uplift, sea-level fluctuations, and climatic shifts, dividing into Western, Central, and Eastern branches by the early Miocene.^[1] The Western Paratethys, centered in the North Alpine Foreland Basin, connected to the Mediterranean until its isolation in the late Early Miocene due to orogenic uplift.^[1] In contrast, the Central Paratethys, spanning the Pannonian and Alpine-Carpathian basins, reached its peak as a marine biodiversity hotspot during the Langhian stage of the Middle Miocene (16.0–13.8 million years ago), hosting over 698 mollusk species under subtropical conditions during the Miocene Climatic Optimum.^[1] The Eastern Paratethys, extending from Ukraine to Kazakhstan, featured deep basins like the Black Sea and South Caspian, characterized by clinoform sedimentation and transgressive-regressive cycles tied to global sea-level changes.^[2] Tectonic reorganization and the Middle Miocene Climatic Transition (around 13.8 million years ago) triggered major environmental upheavals, including salinity crises, basin fragmentation, and mass extinctions such as the Mid-Badenian Extinction Event, which decimated Central Paratethys biota.^[1] By the Late Miocene, profound regressions—such as the terminal Sarmatian event with sea-level drops of 450–500 meters—transformed the system into brackish lakes, including the expansive Lake Pannon, while the Eastern Paratethys persisted with shifting shorelines and endemic faunas until the Pleistocene.^[1]^[2] Modern remnants, such as the Black, Caspian, and Aral Seas, trace their origins to this ancient sea, underscoring its lasting impact on Eurasian paleogeography and hydrology.^[1]

Definition and Historical Context

Etymology and Naming

The term "Paratethys" derives from the Greek prefix "para-," meaning "beside" or "parallel to," combined with "Tethys," the name of the ancient Mesozoic ocean, to signify the northern, parallel epicontinental sea that developed alongside the remnants of the Tethys during the Cenozoic. This nomenclature was coined in 1924 by the Serbian geologist Vladimir Laskarev to describe a distinct biogeographic province characterized by unique Neogene marine and brackish-water faunas and sediments, separate from the Mediterranean Tethys realm.^[3] Paratethys is formally defined as a vast epicontinental sea system that originated from the northern periphery of the Tethys Ocean, spanning from the Oligocene to the Pleistocene, approximately 34 million years ago until the early Pleistocene, with the main marine phases ending around 2.6 million years ago. It encompassed a dynamic series of interconnected basins influenced by tectonic uplift and regression, evolving from open marine conditions to increasingly isolated brackish and lacustrine environments across a region from the Eastern Alps in central Europe to Kazakhstan in Central Asia.^[1] In geological literature, the name "Paratethys" exhibits variations reflecting regional stratigraphic stages and basin-specific phases, such as the Sarmatian Sea for the Middle Miocene (Serravallian) interval marked by widespread brackish-water deposits, and the Pannonian Sea for the Late Miocene lake system in the Pannonian Basin that succeeded the marine Paratethys. These synonyms highlight the progressive fragmentation of the original sea into discrete sub-basins, while the overarching term Paratethys persists for the unified paleogeographic entity.^[1]

Discovery and Key Research Milestones

The geological entity now known as Paratethys was first recognized in the late 19th century through stratigraphic studies of the Alpine and Carpathian regions, where Austrian geologist Eduard Suess identified distinct marine deposits of the Sarmatian stage, highlighting a northern extension of the ancient Tethys Ocean with unique faunal and sedimentary characteristics.^[4] Suess's work in the 1860s and 1870s laid the groundwork for understanding this epicontinental sea as a separate paleogeographic province, differentiated by its isolation and endemic biota from the main Tethys.^[4] The formal term "Paratethys" was coined in 1924 by Serbian geologist Vladimir Laskarev to describe the chain of Neogene basins from the Alps to Central Asia, encompassing these distinctive stratigraphic units.^[3] In the 1920s, Romanian and Hungarian geologists advanced this framework by establishing the Paratethyan chronostratigraphy, defining key regional stages such as the Eggenburgian and Karpatian based on integrated litho- and biostratigraphic correlations across the Central Paratethys.^[5] Pioneering efforts by figures like Hungarian geologist Lajos Lóczy and Romanian stratigrapher Mihai Simionescu emphasized the role of endemic molluscan assemblages in delineating these stages, solidifying Paratethys as a distinct chronostratigraphic realm.^[5] During the 1970s, integration of plate tectonics revolutionized Paratethys research, with Fritz Rögl and colleagues reconstructing its paleogeography as a dynamic response to the Africa-Eurasia collision and resulting basin fragmentation.^[6] Rögl's 1977 analysis of the Middle Miocene salinity crisis linked tectonic isolation to evaporite formations and faunal endemism, providing a plate-tectonic context for the sea's evolution from open marine to lacustrine conditions. This era marked a shift from descriptive stratigraphy to process-oriented models, incorporating global sea-level changes and orogenic uplift. Since the 2000s, seismic profiling and advanced biostratigraphy have refined Paratethys timelines, revealing precise connections between the Central and Eastern realms through high-resolution basin modeling.^[7] In the 2010s, the INQUA Subcommission on European Quaternary Stratigraphy (SEQS) Paratethys working group published key syntheses on stage boundaries, such as the Eggenburgian-Burdigalian transition and Pontian correlations, using integrated magnetostratigraphy and foraminiferal biozonations to date isolation events with uncertainties below 0.5 million years.^[8] These efforts, exemplified by studies on the Badenian-Sarmatian boundary, enhanced global Neogene chronologies by aligning Paratethyan events with the Mediterranean Messinian salinity crisis. Post-2020 molecular and genomic studies have illuminated the evolutionary legacy of Paratethys endemism, tracing genetic divergences in relict species across its successor basins like the Black and Caspian Seas.^[9] For instance, analyses of Ponto-Caspian amphipods and gobies reveal post-Miocene radiations driven by salinity gradients, with DNA barcoding identifying cryptic speciation in over 50% of endemic lineages, underscoring Paratethys as a cradle for modern brackish-water biodiversity.^[10] These interdisciplinary approaches, combining phylogenomics with paleoenvironmental data, highlight ongoing adaptations from Paratethys's megalake phase.^[9]

Geological Formation and Extent

Tectonic Origins

The formation of Paratethys was intrinsically tied to the Alpine-Himalayan orogeny, which arose from the collision between the northward-moving African and Arabian plates and the Eurasian plate, beginning in the Eocene epoch around 50-40 million years ago (Ma). This convergent tectonics progressively constricted the Tethys Ocean, leading to significant regression of its marine waters northward by the late Oligocene, approximately 34 Ma, as the orogenic belt uplifted and fragmented the once-continuous seaway.^[11]^[12] The resulting semi-enclosed Paratethys basin developed between the narrowing Tethys to the south and the emerging North Atlantic to the west, creating a vast inland sea that extended across central and eastern Europe. Subduction zones played a critical role in this process, particularly beneath the Carpathians, where the rollback of subducting slabs facilitated basin subsidence while the overriding Eurasian plate experienced compression. Concurrently, the uplift of surrounding mountain ranges, including the Alps and Dinarides, further isolated the basin through the development of topographic barriers and sediment influx, transforming the open marine environment into a more restricted system.^[11]^[13] Initial isolation of Paratethys occurred around 34 Ma at the Eocene/Oligocene boundary, marking a pivotal shift to endemic conditions, though episodic marine connections persisted through narrow straits such as the Slovenian Corridor. These tectonic dynamics not only defined the basin's early configuration but also set the stage for its subsequent paleogeographic variability.^[12]^[14]

Spatial Boundaries and Connections

The Paratethys, at its maximum extent during the late Miocene, covered an area exceeding 2.8 million square kilometers, stretching westward from the Rhône Valley to the Aral Sea region in the east.^[15] This vast inland sea was delimited to the south by the rising Alpine orogenic belt, to the north by the Carpathian Mountains, and in the southeast by the Pontides and Taurus ranges, forming a complex topographic enclosure that isolated it from surrounding oceanic realms.^[15] Recent paleogeographic reconstructions, incorporating 2020s paleomagnetic data, position the core Paratethys basin between approximately 35° and 45° N latitude, aligning with mid-latitude continental settings influenced by tectonic compression.^[15] The Paratethys encompassed several major sub-basins that reflected its segmented geography. The Western Paratethys included the Vienna Basin, a foreland depression adjacent to the Eastern Alps, while the Central Paratethys dominated the Pannonian Basin system, a back-arc basin amid the Carpathian arc.^[1] Further east, the Eastern Paratethys incorporated precursors to the modern Black Sea, along with depressions extending toward the Caspian and Aral regions, creating a chain of interconnected yet variably restricted water bodies.^[15] Intermittent connections shaped the Paratethys's hydrological regime, with early Miocene links to the Mediterranean established via narrow straits such as the Rhodanian in the western Alpine foredeep and the Volhynian in the northern Carpathian region.^[15] These gateways facilitated episodic marine incursions until tectonic uplift progressively restricted flow by the middle Miocene.^[16] Later, in the Oligocene to early Miocene, eastern outlets through Caspian gateways allowed transient exchanges with the Indo-Pacific realm, evidenced by the influx of thermophilic fauna from southeastern open waters.^[17] Isolation events, driven primarily by orogenic uplift in the surrounding mountain belts, repeatedly severed these links, transforming the Paratethys into a semi-enclosed epicontinental system.^[15]

Paleogeographic Evolution

Early Anoxic Phases

The early anoxic phases of the Paratethys, marking a pivotal shift in its paleoenvironmental evolution, commenced during the late Oligocene Chattian stage (approximately 28–23 Ma), as tectonic isolation from the remnant Tethys Ocean intensified, resulting in stagnant waters across the expansive basin. This isolation restricted water exchange with oxygenated marine realms, fostering density stratification and dysoxic to anoxic bottom conditions that persisted basin-wide.^[18] The Paratethys at this time functioned as an "anoxic giant," comparable in scale to the modern Mediterranean Sea, with its deep basins experiencing prolonged oxygen depletion unlike the more oxygenated conditions in adjacent Tethys remnants.^[18] Key drivers of these anoxic conditions included limited circulation through narrowing gateways, such as the proto-Rhine Graben and Rhone areas, combined with a warm climate that enhanced evaporation and salinity gradients, while nutrient influx from surrounding continental drainage promoted high surface productivity. These factors led to the widespread deposition of finely laminated black shales and sapropels characteristic of the lower Maikop Formation, with organic carbon-rich layers exhibiting total organic carbon (TOC) contents reaching up to 14% in places.^[18] ^[14] The dysoxic bottom waters, extending from the Euxinic to Caspian sub-basins, minimized bioturbation and preserved these organic sediments in low-energy, deep-marine settings.^[18] This "Anoxic Giant" phase not only contrasted sharply with the oxygenated, carbonate-dominated deposits of the Tethys but also laid the foundation for significant hydrocarbon resources, as the thick (up to 2000 m) Maikop shales evolved into prolific source rocks for oil and gas in the Black Sea and South Caspian regions.^[18] ^[19] The organic-rich nature of these deposits, driven by the interplay of restriction and productivity, underscores the unique biogeochemical dynamics of the isolated Paratethys during this interval.^[18]

Transient Open Marine Connections

During the Early Miocene, following periods of isolation-induced anoxia in the late Oligocene Paratethys, transient marine incursions occurred primarily in the Aquitanian to Burdigalian stages (approximately 23–16 Ma), reintroducing oxygenated oceanic waters through western gateways and temporarily restoring normal marine salinities across parts of the Central Paratethys.^[20] These events were most prominent in the western sectors, where incursions entered via straits along the Alpine Foredeep, facilitating influxes from the Mediterranean into the North Alpine Foreland Basin and adjacent areas.^[11] In the eastern extensions, connections extended toward the Carpathian Foredeep, allowing episodic water exchanges that alleviated prior hypoxic conditions in deeper basins.^[20] The mechanisms driving these incursions involved a combination of eustatic sea-level rises during the Early Miocene Climatic Optimum, which elevated global ocean levels by up to 50 meters, and localized tectonic subsidence that deepened potential corridors such as the Carpathian Foredeep and Alpine troughs.^[21] Subsidence in foreland basins created accommodation space for marine flooding, while brief tectonic quiescence prevented immediate closure of these pathways, enabling short-lived connectivity between the Paratethys and open ocean realms.^[22] These dynamic processes contrasted with the ongoing isolation trends driven by Alpine orogeny, resulting in pulsed rather than sustained exchanges.^[20] These connections were ephemeral, lasting on the order of 10^4 to 10^5 years per event, before Miocene uplift in the Alpine-Carpathian belt severed the western straits and promoted renewed basin restriction.^[22] The influxes promoted benthic repopulation by diverse marine organisms, fostering the development of localized carbonate platforms in shallower sectors of the Central Paratethys, such as the Upper Marine Molasse.^[23] Enhanced oxygenation improved ventilation in previously stagnant deeper waters, temporarily boosting primary productivity and supporting faunal diversification before conditions reverted to brackish, low-oxygen states.^[14] Paleontological evidence for these oxygenation events is preserved in shifts of benthic foraminiferal assemblages toward open-marine species, such as increased abundances of Lenticulina inornata and Sigmoilopsis ottnangensis in the Eggenburgian and early Ottnangian deposits of the North Alpine Foreland Basin.^[23] These assemblages indicate well-oxygenated, neritic environments (>100 m depth in some transgressive phases) with normal salinities, replacing earlier dysaerobic, restricted-marine faunas dominated by opportunistic taxa.^[20] Such faunal turnovers, observed in sections like the Ortenburger Meeressande and NH-Beds, directly correlate with the timing of western incursions and underscore their role in reversing anoxic baselines.^[23]

Evaporite and Salt Giant Formations

During the Middle Miocene, the Paratethys experienced a significant hypersaline episode known as the Badenian Salinity Crisis (BSC), spanning approximately 13.8 to 13.4 million years ago (Ma), which marked a precursor to the later Messinian Salinity Crisis in the Mediterranean.^[24] This event resulted from tectonic uplift and damming that restricted marine connections between the Central Paratethys and the Mediterranean Sea, reducing inflow and promoting intense evaporation under arid climatic conditions.^[25] The crisis led to the precipitation of vast evaporite sequences, forming the so-called "Badenian salt giant," a major depositional system comparable in scale to other Miocene salt giants but confined to Paratethyan basins.^[26] The primary evaporite deposits include thick layers of gypsum (anhydrite) and halite, primarily in the Carpathian Foredeep, Pannonian Basin, and precursor Black Sea depressions. In the Carpathian region, the Baden Salt formation exemplifies these accumulations, with halite beds reaching thicknesses of up to 200 meters in eastern sectors, though typical evaporite units range from 30 to 100 meters.^[27] These deposits exhibit lateral continuity across basins, transitioning from basinal halite to marginal gypsum and clastic interbeds, reflecting a drawdown salina environment where seawater influx was episodically supplemented by continental runoff.^[28] Seismic profiling in the Carpathian Foredeep reveals the subsurface geometry of these salt giants, showing wedge-shaped thickenings toward depocenters and diapiric structures from post-depositional halokinesis.^[25] Hypersalinity gradients developed due to restricted circulation and elevated evaporation, fostering sabkha-like marginal settings with supratidal carbonate-evaporite transitions and microbial mat structures.^[29] Borehole data from Polish and Ukrainian sites, including the Wieliczka and Bochnia mines, confirm fluid inclusion temperatures of 20–40°C during halite crystallization, indicative of shallow, warm hypersaline brines.^[30] Recent drilling in the 2020s, such as in the Soltvadkert Trough (Hungary), has extended the known distribution of Badenian evaporites into intra-Carpathian areas, revealing additional halite-gypsum sequences up to 100 meters thick and supporting models of basin-wide aridity.^[31] These findings underscore the BSC's role in reshaping Paratethyan paleogeography through massive salt deposition, with total evaporite volumes estimated in the hundreds of thousands of cubic kilometers across interconnected basins.^[32]

Transition to Megalake Conditions

During the Late Miocene to early Pliocene, spanning the Pannonian and Pontian stages approximately 11 to 5 million years ago, the Paratethys underwent a profound transformation as marine connections to the Mediterranean and Indian Ocean were progressively severed, leading to the dominance of fluvial inputs and a shift toward brackish to freshwater conditions. This closure was primarily driven by tectonic uplift in the surrounding orogenic belts, including the Carpathians and Caucasus, which elevated sills and barriers, isolating the basin system. Preceding hypersaline phases had deposited extensive evaporites that further impeded marine incursions, but by this period, increased riverine discharge overwhelmed residual salt barriers, diluting salinity levels to below 5–8 parts per thousand. In the Eastern Paratethys, similar transitions led to the formation of brackish lakes such as the Akchagyl and Apsheron, precursors to the Caspian Sea.^[2] The resulting "megalake" phase marked the Paratethys's evolution into one of Earth's largest lacustrine systems, with the Pannonian Lake emerging as the dominant feature in the Central Paratethys, covering an expansive area fed primarily by precursors of the Danube, Tisza, and other rivers draining from the surrounding orogens. This lake attained a volume of approximately 80,000 cubic kilometers and depths reaching up to 1 kilometer, creating a vast endorheic basin that trapped freshwater runoff from surrounding highlands.^[33] The system's scale was facilitated by Andean-scale uplift in the encircling orogens, which not only blocked potential outflows but also enhanced sediment delivery through accelerated erosion. Key drivers of this lacustrine expansion included ongoing deltaic progradation, where fluvial sediments progressively filled peripheral basins and reduced the overall water body, while climatic shifts toward wetter conditions in Eurasia boosted riverine influx. By the late Pliocene, around 2.6 million years ago, intensified tectonic fragmentation and regressive sedimentation divided the megalake into separate entities, including the precursors to the Caspian, Black, and Aral seas. This marked the terminal phase of the unified Paratethys lake system, transitioning it toward the modern isolated basins.

Dissolution and Post-Paratethys Legacy

During the Pliocene to Recent period (approximately 5 Ma to present), the remnants of Paratethys experienced progressive fragmentation driven by tectonic subsidence and surface erosion, which facilitated the dissolution of extensive Miocene evaporite deposits known as salt giants. These processes, particularly prominent in the Carpathian Foredeep and Pannonian Basin, led to the development of karst terrains characterized by collapse breccias, sinkholes, and subsidence features resulting from the high solubility of gypsum and halite layers.^[34] In parallel, the dissolution and structural deformation of these evaporites created impermeable barriers and stratigraphic traps essential for hydrocarbon accumulation, as seen in major petroleum provinces across the Paratethyan realm where Badenian salts serve as seals overlying Miocene reservoirs.^[35] The primary legacy basins of Paratethys persist as the Black Sea and Caspian Sea, which represent isolated remnants of the once-vast system. The Black Sea maintains deep anoxic waters, a holdover from the prolonged oxygen-deficient conditions of the late Miocene megalake phase, preserving organic-rich sediments and influencing modern biogeochemistry.^[11] The Caspian Sea, as the world's largest endorheic lake, embodies the final hydrological disconnection from oceanic influences, with its brackish waters and fluctuating levels reflecting ongoing isolation since the Pliocene.^[11] Seismic activity remains active along inherited fault lines bounding these basins, reactivated by continued Alpine-Himalayan convergence and intraplate stresses, contributing to regional tectonics in the circum-Black Sea and Caspian domains.^[11] Contemporary geodynamic processes underscore the enduring influence of Paratethys structures. In the Pannonian Basin, ongoing tectonic subsidence occurs at rates of 1–2 mm/year, driven by lithospheric cooling and sediment loading, which sustains basin inversion and accommodates post-rift sedimentation.^[36] This subsidence, coupled with fluvial erosion, shapes the Danube Delta's progradation, where legacy Paratethys connectivity pathways control sediment distribution and deltaic architecture in the northwestern Black Sea shelf.^[37] Recent 2020s research highlights the vulnerability of Paratethys legacy basins to anthropogenic climate change, with projections indicating that rising sea levels and warming could destabilize methane hydrates in the Black Sea, potentially mirroring Miocene reconnection events that released significant carbon.^[38] Studies modeling anoxic basin responses suggest that subsurface evaporite remnants may modulate local sea-level accommodation through dissolution-enhanced porosity, thereby buffering inundation effects in adjacent marginal seas like the Black and Azov Seas.^[38]

Paleoenvironmental Dynamics

Sedimentary and Climatic Records

The sedimentary record of the Paratethys reveals a complex stratigraphy characterized by cyclic parasequences that reflect repeated shifts in depositional environments, including shales indicative of deeper, anoxic basins, carbonates from shallow marine platforms, and evaporites signaling hypersaline conditions.^[39] These cycles, often on the order of third- and fourth-order sequences, document the basin's response to eustatic sea-level fluctuations and tectonic influences during the Oligocene to Miocene.^[40] Key formations include the Leithakalk, a prominent Middle Miocene carbonate unit dominated by bioclastic limestones and corallinacean-bryozoan buildups in the Central Paratethys, which formed on submerged highs amid siliciclastic influx.^[41] In contrast, the Szolnok Formation represents clastic-dominated turbiditic sands and marls deposited in deeper troughs of the Late Miocene Pannonian Basin, highlighting a transition to more terrestrial sediment sources.^[42] Climatic proxies preserved in these sediments provide evidence of evolving paleoenvironments, with oxygen isotope (δ¹⁸O) values in foraminifera and mollusks showing a shift from warm-wet conditions in the Oligocene, marked by relatively low δ¹⁸O (around -2 to 0‰), to increasingly arid Miocene regimes with elevated δ¹⁸O (up to +3‰ or higher), reflecting reduced precipitation and higher evaporation.^[43] Pollen assemblages from Paratethys margin sites further illustrate this transition, with early Miocene subtropical forests dominated by evergreen broadleaf taxa giving way to mid-Miocene steppe vegetation rich in drought-tolerant herbs and shrubs, such as those from Chenopodiaceae and Poaceae.^[44] Regional variations in these records underscore dynamic influences, including monsoonal precipitation patterns in the early Miocene that enhanced humidity around the proto-Paratethys margins, driven by interactions with the retreating Tethys and emerging Asian monsoon systems.^[45] By approximately 13 Ma, during the Middle Miocene Climate Transition, aridity peaked under Mediterranean-like conditions, as evidenced by intensified evaporite deposition and pollen shifts toward xerophytic communities, linked to Paratethys shrinkage and global cooling.^[46] Carbon isotope (δ¹³C) data from recent studies highlight connections between anoxic events and broader warming episodes, such as the Kuma Anoxic Event in the Middle Eocene, where negative δ¹³C excursions (down to -28‰ in organic matter) coincide with global hyperthermals, promoting widespread deoxygenation and organic carbon burial across the Eastern Paratethys.^[14] These proxies emphasize the basin's role in sequestering carbon during transient warm periods, with quantitative models indicating enhanced stratification that sustained anoxia for millions of years.^[47]

Hydrological and Isotopic Evidence

Strontium (⁸⁷Sr/⁸⁶Sr) and oxygen (δ¹⁸O) isotopes serve as key proxies for tracing marine versus continental water inputs and reconstructing salinity variations in the Paratethys basin. These methods leverage the distinct isotopic signatures of oceanic seawater—typically lower ⁸⁷Sr/⁸⁶Sr ratios around 0.7088–0.7090 during the Miocene due to hydrothermal inputs—and continental runoff, which exhibits higher ratios (~0.7095–0.7120) from weathering of radiogenic crustal rocks. Oxygen isotopes in foraminiferal calcite or biomarkers reflect seawater composition influenced by evaporation (enriching δ¹⁸O) and freshwater dilution (depleting it), with normal marine values near 0‰ and hypersaline or evaporative conditions exceeding +2‰. Hydrogen isotopes (δD) from alkenones provide complementary evidence for evaporation rates, as biosynthetic fractionation leads to enriched δD values (> +50‰ relative to source water) under arid, high-evaporation regimes. Recent advancements, including laser ablation-inductively coupled plasma mass spectrometry (LA-ICP-MS) for in situ analysis of carbonates, have refined spatial resolution of these signals, enabling precise identification of transient inflow events without bulk sample dissolution.^[48]^[49]^[50] In the early stages of Paratethys evolution during the Oligocene to early Miocene, isotopic records indicate predominantly marine signatures, with ⁸⁷Sr/⁸⁶Sr ratios closely matching global seawater values of approximately 0.7090, reflecting open connections to the Tethys and Mediterranean realms. For instance, Badenian (middle Miocene, ~14 Ma) foraminifera from the Central Paratethys yield δ¹⁸O values ranging from -2.1‰ to +1.0‰, consistent with salinities near 35‰ and minimal continental influence. These data suggest a well-mixed, normal-marine hydrology sustained by Atlantic inflows through gateways like the Rhône-Rhine corridor. By the late Miocene, however, strontium ratios shifted toward higher values (~0.7091–0.7095), signaling increasing fluvial dominance from surrounding Alpine and Carpathian river systems, which introduced radiogenic strontium and lowered basin-wide salinity to 20–30‰ in peripheral areas. LA-ICP-MS analyses of ostracod shells from the Dacian Basin (Romania) in the 2020s have pinpointed episodic marine incursions around 7.6–7.4 Ma, with brief drops to 0.70835, corroborating Eastern Paratethys (Black Sea precursor) transgressions that temporarily restored marine-like conditions.^[48]^[49]^[14] Salinity gradients across the Paratethys intensified during evaporite phases, as evidenced by elevated δ¹⁸O and δD values indicating hypersaline conditions. In the middle Miocene Badenian evaporite crisis (~13.8 Ma), Central Paratethys δ¹⁸O spikes to +1.0‰ in benthic foraminifera reflect salinities exceeding 40‰ locally, driven by restricted gateways and high evaporation, while peripheral basins remained brackish at 15–25‰. Hydrogen isotope records from alkenones in the Eastern Paratethys show progressive δD enrichment of up to 80‰ by the late Miocene (~6 Ma), implying aridity and evaporation rates that reduced surface salinities to below 5‰ in isolated sub-basins like the Pontian Sea. These shifts culminated in the Messinian (~5.9–5.3 Ma), where strontium data from the Dacian Basin document a transition to fluvial dominance (⁸⁷Sr/⁸⁶Sr ~0.7098), with salinity gradients from hypersaline cores (>50‰) to freshwater lakes (<5‰) in the north. Gateway reopenings are marked by negative δ¹⁸O excursions (e.g., -1.9‰ around 6.1 Ma), indicating freshwater or low-salinity inflows from the Eastern Paratethys that mitigated evaporative drawdown. Overall, these isotopic trends highlight a progression from marine-dominated hydrology to a continental megafreshwater system by the Pliocene.^[51]^[50]^[48]

Biota and Ecological Insights

Invertebrate Assemblages

The invertebrate assemblages of the Paratethys were dominated by mollusks, foraminifera, and ostracods, which collectively reflected the basin's transition from open marine to increasingly restricted and hypersaline conditions. Mollusks, particularly bivalves of the family Cardiidae such as the endemic Limnocardiinae, formed a major component, with over 220 species evolving in isolation within derived lake systems like Pannon, adapting to brackish and freshwater environments through phyletic evolution and high speciation rates. Foraminifera included bolivinid taxa, which thrived in anoxic bottom waters during depositional phases marked by low oxygen levels, as evidenced by their abundance in the Bolivina-Bulimina zone of early Miocene sediments. Ostracods served as key indicators of salinity fluctuations, with assemblages varying from euryhaline species in marginal settings to more stenohaline forms during transient marine incursions, enabling reconstructions of hydrological changes across the Central and Eastern Paratethys. High endemism characterized these groups due to prolonged isolation following the Eocene-Oligocene separation from the Tethys, with shallow-marine molluscan species reaching 80-85% endemism during the Burdigalian and Serravallian stages. Adaptations included the development of thin-shelled, dwarfed forms among bivalves and gastropods in hypersaline phases, such as those during the Sarmatian, where reduced body sizes facilitated survival in low-oxygen, high-salinity waters. In contrast, open marine phases supported diverse reef-building communities, including coral-associated gastropods and serpulid bioherms that fostered complex invertebrate habitats during the Langhian peak of the Miocene Climate Optimum. Diversification began in the Oligocene, with early assemblages in the Eastern Paratethys showing initial radiations of mollusks and foraminifera amid cooling climates and basin restriction. The Miocene saw peak biodiversity in the early Badenian (Langhian), but salinity swings triggered mass extinctions, notably at the Badenian-Sarmatian boundary (~12.7 Ma), where approximately 98% of gastropod species and around 94% of overall Badenian fauna including bivalves were lost due to dysoxic conditions and hydrological isolation.^[1] Recent studies on microbial mats within Paratethys evaporites, including serpulid-microbialitic bioherms from the upper Sarmatian, reveal integrated benthic communities with cyanobacteria and associated invertebrates, highlighting the role of microbial ecosystems in stabilizing hypersaline substrates.

Vertebrate Fauna

The vertebrate fauna of the Paratethys exhibited significant diversity across major groups including fishes, reptiles, birds, and mammals, shaped by the basin's progressive isolation from the open Tethys Ocean beginning in the Oligocene. Sites such as Máriahalom in the Central Paratethys reveal a mixed assemblage encompassing sharks, crocodiles, aquatic and terrestrial mammals, and birds, reflecting a range of ecologies from fully marine to marginal habitats.^[52] Similarly, the Gratkorn locality in the Styrian Basin documents representatives from all major vertebrate clades, underscoring the region's role as a hotspot for Cenozoic marine and transitional biodiversity.^[53] High endemism, driven by vicariance from tectonic fragmentation and gateway restrictions, characterized later stages, with up to several dozen endemic species in isolated sub-basins.^[54] Ecological roles of Paratethyan vertebrates were integral to the marine food web, with nektonic groups like sharks and cetaceans serving as apex predators that regulated prey populations and facilitated nutrient cycling. For instance, in the Volhynian stage (late Middle Miocene), small-bodied cetaceans such as Kentriodon fuchsii (Kentriodontidae) and Pachyacanthus sp. (Platanistidae) occupied top trophic levels, preying on fishes in open-water environments.^[55] Herbivorous or detritivorous roles were evident among marginal reptiles and birds in shallow, vegetated margins, while overall vertebrate communities responded to anoxic events by favoring epipelagic and pelagic lifestyles, avoiding oxygen-depleted benthic zones that primarily impacted invertebrates.^[14] This integration with invertebrate-based food chains supported the stability of Paratethyan ecosystems during periods of connectivity. Turnover events marked key phases of vertebrate evolution in the Paratethys, with Oligo-Miocene radiations linked to initial basin isolation promoting speciation in endemic clades. Cladistic analyses from the 2020s, including phylogenetic placements of fossil seals, confirm vicariance-driven diversification, such as the stem Phocinae lineage represented by Paratethyphoca libera in the Bessarabian stage (Late Miocene).^[56] In the Pliocene, progressive freshening of remnant basins triggered declines and extinctions among marine-adapted vertebrates, devastating endemic assemblages as hypersaline and lacustrine conditions replaced open-marine habitats.^[57] Transitional faunas, like those of the Volhynian, illustrate re-colonization dynamics post-extinction, blending Central and Eastern Paratethyan elements.^[55]

Fishes and Aquatic Adaptations

The fish fauna of the Paratethys was predominantly composed of teleosts, with over 200 species recorded across its Miocene history, reflecting high diversity in marine, brackish, and freshwater habitats.^[58] Endemic families such as Valenciidae, represented by genera like Miovalencia and new fossil species from Middle Miocene deposits, exemplified localized radiations adapted to coastal and lagoonal environments.^[59] Chondrichthyans, including deep-water forms like those in the Vienna Basin, were present in the Early Miocene but became rare following anoxic events that disrupted marine connections and favored oxygen-sensitive taxa.^[60] In the late phases, particularly during the Maeotian and Pontian stages of the Late Miocene, cyprinids such as those in the Cyprinidae family dominated freshwater assemblages in the Dacian Basin, comprising up to six of seven identified taxa in Romanian sites.^[61] Fish in the Paratethys exhibited morphological adaptations to fluctuating environmental conditions, including low oxygen levels and salinity shifts. Gill remodeling, a common teleost response involving increased surface area or structural changes, enabled survival in hypoxic waters post-anoxic phases, as seen in general patterns among Paratethyan gobioids.^[62] Osmoregulatory adaptations were prominent in euryhaline species like Paratethyan gobies (Gobiidae), which tolerated brackish to freshwater transitions through enhanced ion transport mechanisms in gills and kidneys, facilitating colonization of isolated sub-basins.^[63] In the Late Miocene megalake phase, dwarfism emerged as an evolutionary response in taxa such as dwarf gobies (standard lengths 16–34 mm) from the Eastern Paratethys, likely driven by resource limitation and stable lacustrine conditions in Moldova's Volhynian deposits.^[64] Evolutionary patterns among Paratethyan fishes featured bursts of speciation during the Miocene, driven by allopatric isolation in fragmented sub-basins following the mid-Miocene separation from the Mediterranean.^[65] This vicariance promoted diversification in groups like sand gobies, with crown radiations in the Adriatic and Aegean linked to Paratethyan refugia.^[66] Fossil sites in the Dacian Basin, such as Podari in Dolj County, Romania, have yielded over 50 taxa across multiple localities, including cypriniforms and percids, highlighting endemic bursts in Late Miocene freshwater ecosystems.^[67] Post-2015 genomic studies on descendant lineages, including Caspian Sea carp and Black Sea gobies, reveal rapid adaptive evolution through selection on osmoregulatory genes, underscoring the genetic legacy of Paratethyan isolation.^[68]

Marine and Transitional Mammals

The Paratethys Sea, isolated from the open Tethys Ocean during the Oligocene, became a cradle for endemic radiations of marine mammals, particularly among cetaceans and sirenians. Initial immigrants from the Tethys included early odontocetes and dugongids that dispersed into the newly formed basins around 34 million years ago. Over the Miocene, these groups diversified, encompassing both toothed and baleen whales as well as herbivorous sea cows, reflecting adaptations to progressively restricted and variable salinities.^[69]^[70]^[71] Among cetaceans, endemic forms such as the eurhinodelphinid Praeurhinodelphis stellenbosse exemplified specialized adaptations to the Paratethys environment. This long-snouted dolphin, first recorded in the Central Paratethys during the early Miocene, featured an elongated rostrum suited for capturing prey like fishes in shallow, brackish waters.^[72] Recent CT-scan analyses of inner ear structures from Paratethyan eurhinodelphinids reveal enhanced high-frequency hearing capabilities, indicating advanced echolocation for navigating isolated basins with limited visibility and sound propagation. These adaptations likely facilitated hunting in the confined spaces of the shrinking sea, where endemic baleen whales, such as dwarf cetotheriids, also evolved smaller body sizes—often under 5 meters in length—compared to open-ocean relatives, enabling efficient foraging on abundant local fish populations.^[70] Sirenians, represented by halitheriine dugongids like Metaxytherium medium, similarly underwent endemic evolution in the Paratethys. These herbivorous mammals, widespread across Central Paratethyan waters from the Oligocene to Miocene, developed robust tusks and grinding dentition for seagrass consumption in coastal shallows. As the sea freshened during the late Miocene, some halitheriines tolerated brackish incursions, but their overall body sizes diminished to around 2-3 meters, aiding mobility in narrowing habitats with reduced vegetation. This decline in diversity, from multiple sympatric species in the early Miocene to near absence post-10 million years ago, coincided with the Paratethys's transformation into a megalake, where hypersalinity earlier and subsequent freshening disrupted marine ecosystems.^[73]^[74]^[74] The extinction of most Paratethyan marine mammals around 10 million years ago was primarily linked to escalating freshening and hydrological isolation, which rendered the basins uninhabitable for obligate marine forms. Endemic radiations peaked during the Middle Miocene Climatic Optimum but faltered as water levels dropped and salinity plummeted, eliminating suitable prey bases and stranding populations in fragmented lakes. Surviving lineages were limited to euryhaline species, underscoring the Paratethys's role in driving both innovation and vulnerability in mammalian aquatic adaptations. Recent 2024 studies on dwarf baleen whales further highlight ongoing discoveries of endemic forms as of November 2025.^[15]^[4]^[15]

Significance and Modern Relevance

Economic Resources

The Paratethys deposits host significant hydrocarbon resources, primarily derived from anoxic shales and organic-rich sediments formed during Oligocene to Miocene periods of restricted marine conditions.^[11] These source rocks have contributed to major oil accumulations in the Romanian Carpathians, where cumulative production exceeds 5.3 billion barrels of oil from fields such as those in the Moinești and Prahova sub-basins. In the Pannonian Basin, Middle and Upper Miocene strata serve as key sources for thermogenic gas, with total discovered gas reserves estimated at 5,693 million barrels of oil equivalent across 142 accumulations.^[75] Offshore extensions into the Black Sea, linked to Paratethys paleoenvironments, include the Neptun Deep project with estimated recoverable reserves of 100 billion cubic meters of gas, positioning it as one of Europe's largest untapped fields.^[76] Mineral resources from Paratethys evaporitic sequences are dominated by salt and associated evaporites, with the Miocene Badenian deposits forming extensive "salt giants" through hypersaline lagoonal precipitation.^[77] In Poland, the Wieliczka and Bochnia mines exploit these Miocene rock salt layers, part of a broader national inventory exceeding 107 billion tons of proven reserves, though primarily from older Zechstein with Miocene contributions supporting historical and industrial extraction.^[78] Gypsum, derived from associated evaporite facies, is utilized in construction materials across Central European Paratethys basins, with production from Polish and Ukrainian outcrops providing key inputs for cement and plaster industries.^[79] Potash deposits in the Ukrainian Carpathian Foredeep, formed in Miocene kainite- and langbeinite-bearing layers, represent economically viable resources for fertilizers, with the Kalush and Stebnyk mines historically yielding significant volumes amid regional evaporite basins.^[80] Exploration of Paratethys resources began with 19th-century salt mining in Galicia (modern Poland and Ukraine), where operations in the Wieliczka deposit and Carpathian Foredeep produced 9–13 kg per inhabitant annually by the late 1800s, driving early industrial development.^[81] Hydrocarbon extraction accelerated in the 20th century, with Romanian Carpathian oil fields discovered via conventional drilling from the 1850s, evolving to modern hydraulic fracturing in the Pannonian Basin to access tight gas reservoirs since the 2010s.^[82] Recent EU assessments highlight sustainable extraction challenges, emphasizing integrated management to mitigate impacts on geothermal aquifers and biodiversity in the Pannonian Basin, as outlined in 2021 GeoConnect3D project reports.^[83]

Influence on Contemporary Basins

The Black Sea, as a primary successor basin to the Paratethys, retains a stratified water column with a persistent anoxic deep layer that originated from the stagnation and isolation of the Paratethys during its late Miocene lacustrine phase. This anoxic condition, extending over approximately 87% of the basin's volume below 150 meters depth, stems from restricted deep-water ventilation due to the historical disconnection from open ocean circulation, limiting oxygen exchange and promoting sulfide accumulation.^[11] The resulting low-oxygen environment has profoundly shaped contemporary biodiversity, fostering unique anaerobic microbial communities in the deep waters while restricting multicellular life, and contributing to the overall low diversity in the basin compared to fully oxygenated seas.^[38] Endemic species, particularly in the Ponto-Caspian faunal assemblages derived from Paratethys refugia, dominate certain groups such as ostracods and nannoplankton, reflecting long-term isolation.^[11] The Caspian Sea and Aral Sea, remnants of the Eastern Paratethys, exemplify the endorheic hydrology inherited from the Paratethys's transformation into a closed megalake system around 11.6 million years ago, with no outflow to the ocean leading to salt accumulation and heightened sensitivity to hydrological imbalances. This closed-basin configuration has exacerbated salinity fluctuations, as seen in the Caspian Sea's variable brackish conditions (averaging 1.2% salinity), which support highly specialized ecosystems but render them vulnerable to climatic shifts.^[11] In the Aral Sea, this endorheic legacy amplified human-induced desertification; since the 1960s, diversion of inflowing rivers for irrigation has caused over 90% volume loss and salinity increases from 10 g/L to over 100 g/L in the southern basin, transforming fertile lands into the Aralkum Desert and disrupting aquatic habitats.^[84] Broader geological legacies of the Paratethys influence modern sedimentary dynamics and geohazards across the region. Ancient sediment routing pathways, established during Paratethys infilling with clastic turbidites and evaporites from surrounding orogens, continue to shape deltaic systems like the Danube and Volga, where Miocene depositional patterns control contemporary sediment accretion and coastal morphology.^[11] Inherited tectonic faults from the Paratethys's closure and compression phases contribute to elevated seismic risks, as evidenced by active faulting in the Carpathian and Caucasus margins that underlies modern earthquake-prone zones around the Black and Caspian Seas.^[11] Recent climate models project hydrological alterations under global warming scenarios, with potential for Black Sea freshening from increased river discharge (e.g., Danube inflows rising 10-20% by 2100 under RCP4.5), echoing Paratethys brackish episodes and risking further stratification and ecosystem shifts, as highlighted in IPCC assessments of regional precipitation changes.

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Poland has 19 proven rock salt deposits, with over 85.4 billion tonnes in extra-pillar deposits. Total proven resources are over 107.5 billion tonnes, with ...
[78]
(PDF) Evaporites of Ukraine: A review - ResearchGate
PDF | The results of geological and lithological-geochemical investigations of the Devonian, Permian, Jurassic and Miocene evaporite deposits of Ukraine.
[79]
[PDF] K/Ar DATING OF THE MIOCENE POTASH SALTS OF THE ... - SAV
The major rock- forming minerals of the potash deposits are halite, langbeinite, and kainite.
[80]
SALT MINING IN GALICIA (1867 – 1900)
During the last quarter of the XIXth century 9 – 13 kg of salt was produced per 1 inhabitant, which was twice more than the natural needs of a human being for ...<|separator|>
[81]
The hydrocarbon past, present, and future of Romania—the world's ...
More than 23 300 wells have been drilled in Romania. They have discovered 19.2 billion barrels of oil-in-place and 23.7 trillion ft3 of gas-in-place, and ...<|separator|>
[82]
[PDF] Lessons learnt from the Pannonian Basin case study
Sep 13, 2021 · Another example is hydrocarbon exploitation that might possibly affect geothermal aquifers to some extent. The harmonised management of ...Missing: extraction 2020s
[83]
Past, Present and Future of the Aral Sea -A Review of its Fauna and ...
Like the Caspian Sea and many smaller water bodies in Central Asia, the Aral Sea was brackish with an original mean salinity at 10.3 grams/kg. It is noteworthy ...Missing: Paratethys endorheic legacy