The grandeur of Iguazú Falls in central-eastern South America is vastly enhanced if one looks beyond its stunning beauty. Even though it's a recent addition on the landscape with geomorphology that is simple in construction, its evolution is the product of a long succession and complex interaction of tectonic events and geologic processes that span over a billion years. The revelation adds a depth of color far beyond the visual and enriches our understanding of the natural forces at work that shape our planet.
Part I (here) - From the late Precambrian through the late Mesozoic, three supercontinents in succession endowed the region of Iguazú Falls with a Late Proterozoic crystalline foundation, an overlying Paleozoic sag basin and a capping veneer of Early Cretaceous volcanic rocks.
Part II - The Paraná-Etendeka Volcanic Province has much to tell about the genesis of regional uplift, mass extinctions, mantle dynamics, supercontinental fragmentation and the creation of the South Atlantic realm that set the stage for the creation of the falls in the Pleistocene.
Part III, forthcoming, concludes with a photographic glimpse of the astoundingly rich, bidiverse and colorful rainforest that encompasses the region.
Pertinent definitions are italicized and important names are emphasized in bold. Photographs were taken on a recent visit to the falls in February 2017.
Comparisons of the world's greatest waterfalls invariably include elevations, widths, freefall, flow rates and volume. With a height of 269 feet, width of 9,500 feet and an average volume of 61,660 cfs that pours over a complex of some 275 discrete waterfalls at normal flow, Cataratas del Iguazú in Spanish) or Cataratas do Iguaçu Falls in Portuguese straddling Rio Iguazú on the border of Brazil and Argentina in south-central South America is at or near the top of the list. What's more, it's likely the most spectacular.
Pronounced eee-gwa-ZOO from the native Tupi-Guarini language, it means Great (guassu) Water (y). With an annual mean in excess of 1.5 million visitors in Argentina and Brazil, two-thirds of the falls are on the Argentinian side within 2,500 cu km sister national parks of both countries, all within a 1984-6 UNESCO World Heritage site.
Copy the following co-ordinates into an on-line mapping program such as Google Earth and travel to the brink of Iguazú: 25°41'36.37"S, 54°26'16.33"W
SUMMARY OF POST PART I - THE ASSEMBLY OF GONDWANA
The austral-sprawling supercontinent Gondwana amalgamated in the early Paleozoic from cratonic building blocks largely acquired following the Late Proterozoic disassembly of Rodinia, its massive supercontinental predecessor. In addition to closure of intervening seas and the incorporation of unifying mobile belts (ancient continent-forming, mountain-building orogenies), Gondwana's disparate landmasses came together by ~530 Ma.
Gondwana was sutured together from two landmasses: West Gondwana (present-day South America and Africa) and East Gondwana (Antarctica, Australia, India and Madagascar). Surrounded by the Panthalassic Ocean in the South Hemisphere, it remained insular until the late Paleozoic when it amalgamated with Laurentia (the ancient cratonic core of North America) to form Pangaea, Gondwana's successor.
INHERITED PRECAMBRIAN CRATONIC COMPONENTS MORPH TO PALEOZOIC SAG BASINS
A number of Rodinia-acquired, stable and rigid Archean to Early Proterozoic cratonic fragments (old and stable continental lithosphere) - the Paranapanema block in particular - became conjugate neighbors within Gondwana. Almost from the time of assembly in the Early Cambrian, West Gondwana's margins were accosted by subducting oceanic lithosphere. It resulted in extension within the supercontinent's interior that formed a jigsaw puzzle mosaic of sag basins (aka cratonic, intracratonic, intracontinental basins). Most of the contiguous basins remained associated through a long succession of assembling and disassembling supercontinents.
Assumedly floored by Paranapanema gneissic-granitic crust, the Paraná Basin initiated formation in the Ordovician (red arrow). Minimally deformed and saucer-shaped, the intracratonic-intracontinental basin exhibited crustal thinning and subsidence that began continued through the Cretaceous (Please see post Part I here for more details).
BASIN-FILL, POLYCYCLIC SUPERSEQUENCES
Six supersequences (unconformity-separated, fault-bound, multi-member sedimentary packages at ~10 million year intervals) accumulated within the Paraná Basin. The ~6,000 meter-thick stack was relatively undistorted during most of the Phanerozoic, as subsidence provided the massive accommodation space for deposition.
At first, the Paraná Basin initiated within West Gondwana as an embayment (gulf opening) of the Panthalassa Ocean but became entrapped within the supercontinent's interior, where it remained throughout its history. Basin-fill occurred not only while Gondwana was in the Southern Hemisphere, in tectonic transit across the equator and amalgamated with Pangaea in the late Paleozoic. The supersequences (below) record a host of tectono-climatic lithologies that include shallow marine, coastal and deltaic, fluvial to lacustrine and desert through glacial.
The Paraná's sixth and final supersequence - the Serra Geral Formation (brown stratum) - occurred in the Early Cretaceous. Lavas emanated from fissures fed by a vast system of dikes and sills and blanketed the basin's uppermost sedimentary strata. It's one of the planet's greatest manifestations of continental flood basalts.
It not only ended the basin's protracted fill-history but heralded a period of large scale global tectonic change that continues to this day - the opening of the Atlantic Ocean and dispersal of the world's continents. And most relevant to this post, the process(es) that resulted in the extrusion of the flood basalts uplifted the Paraná Basin and directed its nascent fluvial system continentward. But of course, I'm getting ahead of myself.
THE SERRA GERAL FORMATION
Serra Geral lavas not only flooded the surface of the Paraná Basin in South America but its basinal counterpart in the Etendeka region of western Africa with the Awahab and Tafelberg Formations. Emplacement occurred before West Gondwana rifted apart and the South Atlantic had begun to open. The two-country region is referred to as the Paraná-Etendeka Volcanic Province (purple blob) and includes a number of enigmatic but genetically related volcanic features on the intervening Atlantic seafloor.
THE PARANÁ-ETENDEKA LIP
It's one of the world's largest preserved and well-exposed Large Igneous Provinces (LIP). Earth history has been punctuated with a number of these flood basalt episodes of high volume, short-lived magmatism that don't fit into the current tectonic plate paradigm (Keep reading!). With a present-day volume in excess of 1,500,000 cu km, the timing and duration of Paraná-Etendeka magmatism has been a matter of debate with the main pulse at ~132 to 134 Ma and lasting from ~1 to 17 Ma, which is a relatively short geological interval at either extreme. With the South Atlantic opening between South America and Africa shortly afterward at ~120 Ma, the timing has fueled a number of genetic hypotheses regarding LIPs, rifting, seafloor spreading and even mantle architecture.
Rifting divided the volcanic province with the Paraná Basin receiving 95% of magmatism in Brazil, Argentina, Paraguay and Uruguay and the remainder in Namibia and Angola. The rift-separated provinces consist of nearly coeval and lithological and geochemical counterparts. Volcanic rocks, however, are formed of heterogenous lava packages with distinct architectural, morphological and geochemical differences. What might this imply?
WHAT ARE SERRA GERAL GEOCHEMISTRIES TRYING TO TELL US?
Compositionally, they're basalts and basaltic andesites (97.5%) with minor quantities of acidic rhyolites (2.5%). Typical of many LIPs where silicic components are often present, Paraná-Etendeka's rhyolitic rocks (pink map regions above) are located near southeastern South America's and southwestern Africa's continental margins from its pre-rift locale.
Together, they cover the bimodal compositional spectrum (red ellipse below) from mafic ("basic"/basaltic) to felsic ("acidic"/granitic) igneous rocks. The association is not unique to the Paraná-Etendeka Province, which is an extensional, mafic-dominated, continental rift regime. Bimodality is also recognized in a number of tectonic settings such as collisional felsic-dominated subduction zones. And, there's more!
In two distinct regions within the Paraná-Etendeka Volcanic Province, tholeiitic basalts (the most common volcanic rock and produced at mid-ocean ridges and continental rifts) exhibit two chemically similar subtypes that overlap temporally and spatially: a low-TiO2 lava field in the south and high-TiO2 in the north (blue and green regions above). The northern phase appears younger than the southern and Etendeka, which is also stratigraphically demonstrable. What is the genetic implication of the subtypes and their distribution?
MORE QUESTIONS (MANY WITHOUT ANSWERS)
There are a number of explanations for the origin of LIPs, the wide range of magma chemical compositions and source of magmatism such as plumes, hotspots, mantle or crustal sources and decompression melting. Regardless of the diverse theories, continental volcanic margins exhibit thinning and extension that led to break-up, seafloor spreading, the formation of oceanic crust and passive margins on the continents that of the newly formed Atlantic realm.
• What mantle process(es) explains Serra Geral geochemistries, distribution, timing and duration of emplacement?
• Does bimodality suggest a single volcanic source?
• Did LIP emplacement trigger rifting and South Atlantic opening? On a grander scale, is the process responsible for the break-up of Pangaea and opening of the North and Central Atlantic?
• What are some of the mantle models for Paraná-Etendeka magmatism? Was magmatism attributable to decompression (upwelling magma-melting due to less pressure), conductive heating or the ascent of an asthenospheric plume that triggered lithospheric mantle melting?
• Does partial melting (a portion of solid rock melts and forms minerals different from the solid) of coevally emplaced basaltic rocks explain the presence of silicic rocks?
• Both basaltic and alkaline igneous complexes are asymmetrically distributed across the LIP, while silicic magmatism is more symmetrical at the site of continental break-up. Does it suggest a link to lithospheric extension?
• What does the V-shaped orientation of seafloor magmatism imply about the process that formed them? If the South American and Africa plates are diverging, why aren't the ridges aligned linearly?
• Does the LIP's south to north age progression of magmatism reflect the direction of rifting?
|What's Down There?|
THE TRISTAN DA CUNHA MANTLE PLUME - HEAT OR MELT SOURCE?
Although not without controversy, the consensus is that the Paraná-Etendeka LIP was fed by the Tristan mantle plume. Its name is derived from the Tristan da Cunha volcanic island group and adjacent Gough Islands. They are located some 500 miles east of the South Mid-Atlantic Ridge spreading center, the divergent boundary between the North American and Eurasian plates) where the plume is currently thought to reside. They are all associated with the opening of the Atlantic and represent a single genetic province some 9,000 km broad.
The Paraná and Etendeka LIP includes two V-shaped, aseismic (without seafloor spreading or earthquakes except at the hotspot) submarine volcanic chains on opposite sides of the Mid-Atlantic Ridge. They are the NW-oriented Rio Grande Rise on the west and NE-oriented Walvis Ridge to the east, respectively on the South American and African Plates. The assumption is they all arose from a single source - a deep mantle plume.
THE PLUME HYPOTHESIS (IN SIMPLE TERMS)
The majority of volcanoes are located at plate boundaries - mid-ocean ridges and subduction zones. About 5% are within plates such as the Hawaiian Islands. The magmatism is classified as a hotspot, stationary, time-progressive regions of local surface volcanism. Some are coincident with or near mid-ocean ridges - such as Iceland and the Paraná-Etendeka LIP - and are thought by many to be produced by mantle plumes.
Hotspots and the Plume hypothesis have become incorporated into Tuzo Wilson's almost universally accepted 1960s Theory of Plate Tectonics (a rigid outer lithospheric layer glides over a plastic, partially molten asthenospheric layer). It provides a mechanism for continent assembly and disassembly and volcanism both at plate boundaries, while convective upwellings of the Plume hypothesis account for volcanism elsewhere such as at the Emperor-Hawaii ridge within the Pacific plate. Since its inception by Morgan in 1971, the 20 initially identified have ballooned to about 122, although the record is 5,200.
Plumes are deep-seated (sub-lithospheric), fixed (spatially persistent in location), diapirs (narrow vertical upwelling columns of unusually hot (but not molten due to extreme pressure), mantle-derived material that is heated by the Earth's core. Plumes are thought to originate from the core-mantle boundary and buoyantly ascend to the asthenosphere-lithosphere boundary where they produce a high rate of hotspot volcanism at the surface.
In concert with the descent of subducting lithosphere, plumes drive plate tectonics, explain flood basalts on land and sea, produce unidirectional time-progressive volcanic chains and even break up supercontinents forming new oceans! It's a grand picture that explains the genesis of the Hawaiian Island system and was actually inspired by it.
The concept makes great sense (but not to everyone). Why is there no evidence of plume-induced precursory uplift, flood basalts and a hotspot conduit beneath the volcanically active Big Island? How can the chain's "bend" and time-progression possibly occur given slow plate movement? Why do geochemical signatures indicate a shallow mantle source? Why are there are no reliable seismic tomographic images, only computer models?
THE TRISTAN PLUME - THE DRIVING FORCE IN WEST GONDWANA BREAK-UP
At the top of its ascent, a plume head is thought to flatten into a 2,000 to 2,500 km disk and enter a continent's spreading center where eruptive products generate a hotspot. Beneath the continent, magma becomes molten due to adiabatic decompression (decreased pressure due to ascent without heat transfer, raising temperatures or adding flux like water). Basaltic magma then penetrates the crust and is influenced by it. As it melts, it fractionally crystallizes (Bowen's process whereby magma differentiates into a progression of igneous rock types as it cools).
Initially, it is thought that plumes actively force a continent apart and more recently, thermally and chemically erode the base of the lithosphere and promote a melt that exacerbates lithospheric weakening. The process is thought to account for Paraná-Etendeka bimodality and geochemistry of rocks of lower mantle origin versus basalts of mid-ocean ridges that are asthenospheric in origin (higher mantle) that develop by partial melting (the chemical differentiation of crustal rocks).
The Tristan plume head is thought to cause domal uplift followed by crustal extension and flood basalts at the plume tail. The formation of seafloor ridges on a time-progressive track, continental break-up of West Gondwana and the opening of the South Atlantic ensues. Paraná-Etendeka basalts erupted just ~5 Ma before seafloor spreading started. The timing of voluminous magmatism and the LIP preceding the opening of the South Atlantic as well as the geochemistries seem to fit, but the concept is not without opposition.
The Plume hypothesis is challenged by a number of anti-plume alternatives. One is edge-driven by changing plate boundaries on continental margins with slab-pull that stretches the lithosphere and initiates rifting. Another contends that the Plume hypothesis has more difficulties than certainties and relies on ad "hoc variants" and contrived modifications for any given situation. Proof is over 70 colorful plume types such as singles, clusters, superplumes, cactoplumes, fossil plumes, stealth plumes, dying plumes, finger plumes, baby plumes, pulsing plumes and even spaghetti plumes.
The Plate hypothesis contends that the location of volcanism and plumes are "inconsistent with many first-order observations" (Foulger) such as a lack of evidence for geophysical indicators (mantle temperatures, time-progressive volcanic tracks or seismic anomalies in the lower mantle). They believe hotspots aren't there or are even needed!
|"The cactoplume – the ultimate fix for any surface phenomenon"|
From mantleplumes.org by platist Erik Lundin
Rather than being contrived as an adjunct to the tectonic plate hypothesis, the Plate hypothesis is fully in keeping with it and simply postulates that "anomalous volcanism" results from lithospheric extension. Thus, melts are permitted to passively ascend from the asthenosphere. It is the conceptual opposite of the Plume hypothesis in stating that volcanism is a shallow, near-surface process not a deep-seated plumal one and that it is a consequence of lithospheric processes rather than an active driver of them.
In other words, like a rift valley that permits melts to ascend from shallow depths, intraplate surface magmatism is explained as a passive response to the stretching of lithospheric plates.
THE PLATIST VIEW OF SOUTH ATLANTIC OPENING
Platists disavow that the Tristan plume severed the West Gondwana continent and opened the South Atlantic. Instead, they believe the northward-propagating mid-ocean ridge crossed a preexisting zone of weakness - a major transtensional intracontinental structural discontinuity with prior rifting history - the Paraná-Chacos basin shear zone between the Paraná and Chacos Basins (See Part I). Some interpret it as a failed rift arm of a triple plate junction where magmatism was focused. The assumption is in keeping with the Plate hypothesis that operates under the geologically established premise that ancient collision zones may re-activate and transform into regions of extension with associated magmatism.
Non-plumists believe that a plume head was not a driving force in the opening of the South Atlantic or even existed during its opening. In addition, anomalous mantle melting occurred only locally. In fact, its purported size is surprisingly small in comparison to the oft-cited diameters of plume heads. What's more, its location is poorly constrained with some placing its location near the Paraná flood basalts and others at the African plate.
THE PLATISTS' VIEW OF THE NORTH ATLANTIC
They believe the Paraná-Etendeka LIP in the South Atlantic is one of many examples of plumeless magmatism. A similar scenario explains the evolution of Iceland in the North Atlantic, where it is almost universally assumed to be underlain by an ascending hot plume from deep within the mantle. Instead, platists believe that Iceland's presence is explained as a natural consequence of relatively shallow processes related to tectonics.
|Conceptual Schematic of the Icelandic Plume|
Iceland lies where the Mid-Atlantic Ridge crosses subducting crust of the Caledonian suture, a structural discontinuity of the disintegrating Pangaean supercontinent. It formed ~400 Ma by closure of the Iapetus Ocean when Baltica (Greenland and Scandinavia) collided with northern Laurentia (in concert with Avalonia's collision with southern Laurentia). Its re-activation permits the ascent of magma from the shallow, upper mantle and results in the formation of the island in the Mid-Atlantic at sea level. There's no need for plumes, if hotspots don't exist.
V-SHAPED SEAFLOOR GEOMETRY EXPLAINED TWO WAYS
Getting back to the Paraná-Etendeka's enigmatic V-shaped seafloor ridges, plumists attribute their geometry to northerly components of three diverging oceanic plates (called an RRR junction) that formed over the Tristan plume. Platists, on the other hand, believe the ridges formed via the accommodation of stress in the lithosphere due to rifting. Release may have occurred along several transform fault segments or failed rift arms or from remelting of detached continental lithospheric mantle. The orientation developed as the South American and African plates diverged, while following a relative track to the NW and NE along arms.
In addition to mantle dynamics and genesis, the Paraná-Etendeka Province finds itself in the midst of another controversy, one involving an enigmatic extinction-volcanism association.
DID THE LIP TRIGGER A MASS EXTINCTION OR MERELY A MINOR BIOTIC CRISIS?
The crux is a near-perfect temporal association between mass extinction events, catastrophic global climate change and at least a half-dozen LIP eruptions of massive basalts in the Phanerozoic with rapid magma extrusion rates. No other phenomenon indicates such a high correlation, even bolide impacts. The most compelling and dramatic are the end-Permian Siberian Traps and Deccan Traps in India. Although coincidence doesn't prove causality, the frequency of a volcanism-extinction connection is compelling.
Typical of the many continental LIPs in the mid-Phanerozoic, the Paraná-Etendeka's vast surface outpourings emplaced over a short geological time frame, although the duration is only variably constrained. Considering the magnitude of the eruption, which is thought comparable to other LIPs associated with mass extinctions, massive volumes of atmospheric gases were likely released with a strong potential for adverse environmental impact. Yet, the LIP has fostered little attention, since it appears to have formed when extinction magnitudes were low. What's up?
All that may change with the discovery of Early Cretaceous Valanginian age (~137 to 132 Ma) black shales in pelagic (bottom) sediments of the Tethysan oceanic realm (that opened in eastern Pangaea before break-up). They reveal major positive δ13C perturbations of the global carbon cycle, the earliest of the Cretaceous system, and a warmer climate. The shales suggest a biocalcification crisis of nannoplanktons that best tolerate low nutrient conditions.
Volcanic activity coincident with the Paraná-Etendeka LIP, prior to the break-up of West Gondwana, may have played a major role in this environmental change by increasing adversely tolerated nutrient conditions, ocean acidification or both via outpouring of bio-limiting atmospheric gases from the mid-ocean spreading center. The crisis may be tied to a global episode of anoxic (oxygen-poor) ocean deposition called the Weissert Event.
If no extinction occurred, it may be due to emplacement over a shorter timescale or lower volatile concentrations or less deleterious ones, fluorine and chlorine in particular that degrade the UV-shielding ozone layer and cause ecosystem stress. It may even be due to the age and composition of the underlying mantle. The Paraná-Etendeka erupted through thermally eroded Proterozoic lithosphere versus the Central Atlantic Magmatic LIP and Deccan Traps, both with high extinction correlations that emplaced through Archean cratonic lithosphere and releasing atmospheric sulfur (above graph).
A NUMBER OF UPLIFTING EXPERIENCES
Thus far, the Paraná intracratonic sag basin formed in West Gondwana in the Ordovician first as an embayment and later became landlocked within the continent's interior. The subduction of Panthalassa oceanic lithosphere along the continent's southwest margin resulted in intracontinental extension and basin subsidence that provided accommodation space within the Paraná Basin for a thick stack of sedimentary supersequences.
The emplacement of Serra Geral continental flood basalts in the Early Cretaceous, whether from hotspot activity or alternative genetic origin, terminated the basin's protracted depositional history and gave rise to the Paraná-Etendeka Volcanic Province, one of the largest in the world. The event was a precursor to rifting that fragmented West Gondwana into South America and Africa and the opened the Atlantic.
Marginal oceanic slab compression not only induced intracontinental extension within the Paraná Basin but caused uplift at various intervals in the Paleozoic. The most significant is thought to have occurred prior to rifting, when the basin was also tilted down to the west and segmented into a succession of three "compartimentos" or planalto (plateaus).
The three plateaus of Paraná are separated by escarpments that progressively expose younger strata of the basin's billion-year history. The First Planalto is formed by igneous and metamorphic rocks with Serra do Mar its eastern boundary. The Second constitutes outcrops of uppermost Paleozoic supersequences sediments that is overlapped by Serra Geral volcanics of the Third. Quaternary sediments occur in all regions especially river valleys. A third subbasin exists in the northwest with
|West to East Schematic Cross-section of the |
Modified from sanderlei.com
DEVELOPMENT OF THE PARANÁ RIVER SYSTEM AND TRIBUTARY IGUAZÚ
Although poorly understood despite its long history and highly controversial, the river system assuredly began to develop concurrent with the rifting process. Megadomal rift-arches developed centrifugal drainage patterns that remain partially evident on the landscape, but the history of the modern system didn't begin until the complete break-up of Gondwana.
Initially, as South America and Africa broke apart, a single, large, longitudinally elongated basin - the Afro-Brazilian Depression - captured drainages and gave rise to an interconnected lake system. The two continents became separated at the end of the middle Cretaceous between 98 and 93 Ma. Following Gondwana break-up, erosive denudation of the uplifting Brazilian crystalline shield occurred as grabens (subsiding rift-blocks) formed offshore sedimentary basins (such as the Santos and Spirito in southeastern Brazil) while isostatic uplift may have occurred in the Sierra do Mar or possibly also related to Mid-Ocean Ridge "push" and far-field Andean orogenic slab "pull.
Uplifted rift-blocks resulted in isolated endorheic drainages (closed basins without outlet) that extended continentward under arid to semi-arid conditions (evidenced by a vast sand sea across southeastern Brazil that directly underlies Serra Geral basalts) probably were the first evidence of a fluvial system.
Concomitant with rifting and uplift into the Neogene, onshore basins became separated from coastal drainage systems on the newly-formed, "Atlantic-style" passive margin by the uplifted, fault-scarped, coast-paralleling, 1,500 mile-long Serra do Mar hydrologic divide. Its eastern escarpment (above) initiated E-W erosive retreat concomitant with deformation that further delineated the evolution of drainage patterns in addition to the capture of surrounding headwaters from adjacent hydrographic systems. The current drainage system developed between the Miocene and Pliocene, concomitant with the initiation of the modern Paraná system.
JOURNEY OF RIO IGUAZÚ
Numerous contemporary rivers headwater within the west flank of the Brazilian Highlands as does Rio Iguazú that originates within Serra da Baitaca State Park. It is directed to the west by basinal tilt, many faults and old and deep episodically active NW-SE, E-W and NE-SW structural lineaments re-activated during Gondwana break-up.
Patterns of topography and drainages, block faulting and river capture provide suggestive evidence of more recent uplift such as from neotectonic (Neogene) compression from far-field stresses from the Andean orogeny in the Miocene, all of which likely contributing to the reorganization of the fluvial basin to the morphology we see today.
It completes a ~1,320 mile, cuesta-escarpment and waterfall-punctuated journey as the river and its floodplain meanders cratonward across sedimentary and volcanic rocks of the Paraná Basin's three plateaus. After cascading off Serra Geral basalts of the Third Plateau at Iguazú Falls, the river joins mainstem Rio Paraná as a left-hand tributary at the Triple Frontier, the confluence of Uruguay, Brazil and Argentina. The system's collective waters reach the Atlantic at the estuary-delta Rio de la Plata between the cities of Montevideo, Uruguay and Buenos Aires, Argentina.
Iguazú Falls is the largest waterfall of the Paraná River Basin, although prior to 1982, it was rivaled by Sete Quesdas. The series of seven waterfalls, also on the Serra Geral Formation, was inundated by the impoundment of the locally controversial and largest in the world Itaipo Reservoir and Hydroelectric Dam upstream on the Paraná River in 1982.
To be discussed, notice that following a dramatic bend in the serpentine river channel immediately above Iguazú Falls (below), the otherwise broad river curiously undertakes a near reversal of direction, while below the falls, it constricts into a narrow gorge that strikes linearly away from a U-shaped chasm called the Devils Throat (tiny white spray).
Where does all that water go? Downriver, Rio Paraná is joined by Rios Paraguay and then Rio Uruguay before emptying into the Atlantic Ocean at Rio de la Plata between Buenos Aires, Argentina and Montevideo, Uruguay.
|The Mainstem Paraná River and Wide Floodplain below the Confluence with Iguazú River|
Directly above the falls, Rio Iguazú is known as Iguazú Superior, where it flows over a number of small steps carved into basaltic bedrock and skirts a slew of small vegetated islands set precariously in the channel. In the midst of initiating another clockwise meander, the river channel dramatically shallows and widens to 1,500 m, as if doubling back on itself.
Paseo Graganta del Diablo, the metallic catwalk above the falls that is reached by taking a short train ride from the visitor center, leads you to the chasm from island to island. With every approaching step the roar of the falls grows louder. Colorful birds and butterflies are everywhere.
THROAT OF THE DEVIL
Frothy, brilliant white and churning violently, about half the river's flow plunges off the volcanic plateau in a huge 2.7 km arc from Argentina to Brazil, while sending a cloud of spray skyward that's visible from space. At the brink, a large portion of Iguazú Superior converges into an enormous mist-shrouded, thunderous funnel that's 230 feet high. Called Garganta del Diablo in Spanish or Throat of the Devil. Curiously, it aligns with the strike of the river channel and gorge downstream from the falls, which is best seen from the air or on map view.
|Staring into the Throat of the Devil|
Shouting to be heard over the roar, the spray is welcomed relief in the 90 degree heat.
Below the falls, Iguazú Inferior tumples into a broad, shallow plungebool that is littered with large blocks of displaced basalt. The channel has completed a hair-pin reversal of direction as it converts to a linear, narrow (~80-90 m) and deep gorge (~70 m) that is somewhat steeper along the north, right bank (below). The channel-chasm-gorge morphology begs the question, what structural aspects caused the river to double back on itself and contribute to the distinctive upfalls and downsfalls morphology?
Oblivious to the turbulence of the falls it has just experienced, Iguazú Inferior calmly flows away in a linear and relatively narrow gorge. It will soon join parent Rio Paraná at the three country confluence.
THE MOST IMPORTANT INGREDIENT
About 20,000 years ago, the regional climate changed for the last time from cold and dry to hot and rainy, But, the continental rainfall regime in southeastern and southern Brazil is a result of moisture from the Amazon to the north. Interacting with cold masses from the south accounts for the Paraná Basin's high rainfall. Of the major tributaries of the Parana River - the Paranaíba, Grande, Tietê, Paranpanema and Iguazú- the latter's importance to the system is based on its drainage basin of 62,000 sq km, length of 1,320 km and an annual mean volume of 1,746 cu m/s. Thus, it has great capacity to generate exceptional discharge (a maximum of 12,799 cu m/s), the lifeblood of the falls.
Although subtropical, unlike many other South American rivers where annual temperature variations are relatively limited, the volume, color and content of Iguazú's waters vary considerably with season. During summer rains from October to March, the reverse of the North Hemisphere, the river swells within its channel and becomes laden with silt and clay from basaltic red soils stained with oxidized iron and aluminum acquired from basaltic mafic minerals - largely pyroxene, feldspar, hornblende, mica and magnetite.
|Wide, Calm, Turbid and Meandering, a Swollen Rio Iguazú Superior Approaches the Falls in the Wet Season|
The region's soils, called latosols that typically develop in tropical rainforests, form from the same minerals. They endow the region with its fertile, deeply colored "red earth " known as "tierra roja" in Argentina and "terra roxa" in Brazil and promote its agricultural bounty beginning with coffee in colonial times.
CLIMATIC VARIABILITY AND EXTREMES
In the dry, winter season from April to July, Rio Iguazú transports a relatively low quantity of suspended sediment, running clear or slightly greenish and unhurried within a moderately wide, basalt-floored, shallow channel across the gently downwest-sloping Paraná Plateau. During these times to the joy of millions that visit it, water copiously spills off the Paraná plateau at ~1,500 cu ft/s. It's a jaw-dropping spectacle for all the senses that visitors can't get enough of!
During an extreme drought in May and June of 1978, the falls actually dried up completely for 28 days due to nonexistent flow. In contrast, 2014 rains in the Argentine and Brazilian regions of Misiones and Paraná reached historic levels that resulted in a flow rate of 46,300 cubic meters per second - 33 times the usual flow rate. The previous record of 36,000 was reached in 1992. Both times, officials closed the catwalks for safety as the discharge completely obliterated the falls within a single wall of murky-brown water.
|Iguazú Falls During Extreme Drought and Overflow of Biblical Proportions|
Modified from airpano.com
GEOMORPHOLOGY OF IGUAZÚ FALLS
Iguazú's construction is surprisingly simplistic in light of the billion year-plus processes that contributed to its formation. Essentially, three uppermost layers of Serra Geral lava give rise to a two-step staircase effect. At normal rates of flow, the system consists of some 275 individual waterfalls, although the number fluctuates from 150 to 300. About half the river funnels into Garganta del Diablo that lies on strike with Iguazú Canyon below the falls. The remainder spills over a curvilinear front that lies perpendicular at the apex of the channel's sweeping, clockwise turn. The falls of San Martin, Adam and Eva, Penoni, and Bergano are the largest of the individual waterfalls along the front.
The explanation for the linear geometry of the gorge and chasm is a NNW to NW intraformational, of which there are a number locally that strike N 80° and N 170°. Large-scale structural controls also exist from re-activated NW and WNW lineaments and epeirogenic (unwarping) since the Pliocene-Pleistocene that mobilizes large-scale blocks.
As one might expect, waterfalls form slower in erosion-resistant, homogenous, stratified bedrock-channeled rivers such as the igneous rocks of the plateau. Characteristically, trapps (or trapps, Swedish for "stairway" in mafic rock) form that are controlled by bed thickness, degree of consolidation, bedding plane discontinuities, joints and fractures.
|Schematic Profile of Iguazú Falls|
Surfaced with vesicular basalt, two traps control the falls' staircase morphology.
From the Argentine side, the lava flows can be seen laterally in the system of prismatic, horizontally fractured, vertical columnar jointing in the vegetated walls of Isla de San Martin, the blocky island below the falls. It displays the lower two of the plateau's superficial-most three basalt flows against a background of the falls' three flows.
|Movie goers will recognize the island and waterfall from The Mission filmed in 1986. |
A species of Black Vultures calls the island home.
One of the most conspicuous and yet not completely understood features occurs along downcutting bedrock-floored channels such as found on the volcanic plateau. Knickpoints, rapids and waterfalls form at an abrupt break or sharp change in slope in longitudinal channel profiles that dip upstream. In conjunction with bedrock erosion (degradation), the knickpoint and waterfall retreat upstream (headward migration). Upstream advancement occurs as blocks of bedrock are hydraulically plucked (quarried) from the lip of the falls by material travelling as bedload (versus suspended load).
Channel incision typically occurs as a flowing body of water finds its way to the lowest point to which it can flow (base level) on the way to the sea. The process is facilitated by climatic change, tectonism, bed lithology, stream kinetic energy and entrained load. Quarrying is the most rapid means of eroding a bedrock channel and is facilitated by hydraulic wedging (where clasts forcefully ratchet apart fractures and joints).
Undercutting of the waterfall cliff (headwall) from rocks that scour and abrade the riverbed at the plungepool (deep depression in the streambed below the falls) causes collapse of the knickpoint lip. It occurs more readily when erosionally susceptible rock (footrock) underlies the strata at the lip (caprock).
As the waterfall retreats, a gorge (80-90 m wide and 70-80 m deep) typically develops in the channel downstream, linear in the case of Iguazú as it follows a fault along the edge of the volcanic plateau. The entire process of waterfall evolution occurs in the youthful stage of river development, which typically occurs in a river system's upper reaches where gradients and channel slopes are greater (oversteepened), water supply is more abundant and flow velocities are faster.
Cylindrical holes in the riverbed above and below the falls form when repetitive current eddies cause sediment and pebbles to abrade the bed. The action progressively exposes pothole walls by keyholing (from below) and incising (from above). Their consolidation promotes vertical and lateral channel incision, headward migration and knickpoint advancement. River polish and fluting commonly occurs on resistant bedrock surfaces.
The pothole remnant in the gorge's wall below the falls has been progressively exposed by channel quarrying to the extent that it reveals its structure laterally. Abandoned potholes and plungepools provide evidence of upstream retreat and when linear, imply the direction of flow. Notice the stratigraphy of the flows in the transected wall. Characteristically, basalt forms a columnar jointing pattern upon cooling, which, when supplemented by horizontal fractures, facilitates channel excavation and waterfall formation.
|Fully incised Pothole|
It's currently thought that, at least since the Pleistocene, Iguazú Falls has been advancing upstream from the confluence of Rios Iguazú and Paraná by headward erosion and knickpoint retreat some 21 km to its present-day location at Garganta del Diablo. The rate is estimated to be 1.4 to 2.1 cm/yr over the last 1.5 to 2 million years.
Many waterfalls of the Paraná River's tributaries have succumbed to the needs of the region's growing population and have been eliminated by hydroelectric projects and dams. It leaves Iguazú Falls as a poignant last example of the greatest falls of the river system. Fortunately, this precious resource remains protected within the two national parks and UNESCO World Heritage site.
In this post, I've attempted to show there is often far more to a landscape or landform than meets the eye. And, that by looking deeper - both in time and space - the revelation adds a profound dimension of richness and enhances our understanding of the natural forces at work that shape our planet.
I am extremely grateful to Edgardo M. Latrubesse, PhD of the University of Texas at Austin and Professor Eduardo Salamuni, PhD of the Federal University of Parana State in Brazil, who contributed extremely helpful information regarding the evolution of the Paraná Basin and geomorphology of Iguazú Falls. Dr. Salamuni's personal communications were of great value in formulating many of the ideas found in this post. Special thanks are also in order for his addition of my blog to his Facebook page (here).
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