The Campanian Ignimbrite eruption was a major volcanic eruption in the Mediterranean during the late Quaternary, classified at 7 on the Volcanic Explosivity Index. The event has been attributed to the Archiflegreo volcano, the caldera of the Phlegraean Fields, located west of Mount Vesuvius under the western outskirts of the city of Naples and the Gulf of Pozzuoli, Italy. Estimates of the date, magnitude and the amount of ejected material have varied considerably during several centuries of investigation. This applies to most significant volcanic events that originated in the Campanian Plain, as it is one of the most complex volcanic structures in the world. However, continued research, advancing methods and accumulation of volcanological, geochronological, and geochemical data has amounted to ever more precise dating. The most recent dating determines the eruption event at 39,280±110 years BP and results of 3D Ash Dispersion Modelling published in 2012 concluded a dense-rock equivalent of and emissions dispersed over an area of around. The accuracy of these numbers is of significance for marine geologists, climatologists, palaeontologists, paleo-anthropologists and researchers of related fields as the event coincides with a number of global and local phenomena, such as widespread discontinuities in archaeological sequences, climatic oscillations and biocultural modifications.
The Phlegraean Fields caldera is a nested structure with a diameter of around. It is composed of the older Campanian Ignimbrite caldera, the younger Neapolitan Yellow Tuff caldera and widely scattered sub-aerial and submarine vents from which the most recent eruptions have originated. The Fields sit upon a Pliocene - Quaternary Extensional domain with faults, that run North-East to South-West and North-West to South-East from the margin of the Apenninethrust belt. The sequence of deformation has been subdivided into three periods.
Phlegraean Periods
The First Period, which includes the Campanian Ignimbrite Eruption was the most decisive era in the Phlegraean Fields' geologic history. Beginning more than 40,000 years ago as the external caldera formed, subsequent caldera collapses and repeated volcanic activity took place within a limited area.
During the Second Period, the smaller Neapolitan Yellow Tuff eruption took place around 15,000 years ago.
Eruptions of the Third Period occurred during three intervals between 15,000 and 9500 years ago, 8600 and 8200 years ago and from 4800 to 3800 years ago.
The structure's magma chamber remains active as there apparently are solfataras, hot springs, gas emissions and frequent episodes of large-scale up- and downlift ground deformation do occur. In 2008 it was discovered that the Phlegraean Fields and Mount Vesuvius have a common magma chamber at a depth of. The region's volcanic nature has been recognized since Antiquity, investigated and studied for many centuries. Methodical scientific research began in the late 19th century. The yellow tuff stone was extensively quarried for centuries, which left large underground cavities that served as aqueducts and cisterns for the collection of rain water. In 2016 Italian Volcanologists announced plans to drill a probe deep into the Phlegraean Fields several years after the 2008 Campi Flegrei Deep Drilling Project which had aimed to drill a diagonal borehole in order to bring up rock samples and install seismic equipment. The project was suspended in 2010 due to safety problems.
Eruptive sequence
The CI eruption has been interpreted as the largest volcanic eruption of the past 200,000 years in Europe. Tephra deposits indicate two distinct plume forming phases, a Plinian and a co-ignimbrite, characterized by multiple caldera-forming eruptions.
Plinian phase
Evidence shows that the eruption was a single event lasting 2 to 4 days. It was triggered by abrupt changes in composition, properties and physical state in the melt or overpressure in the magma chamber. The eruption started with phreatomagmatic explosions, followed by a Plinian eruption column, fed by simultaneous extraction of two magma layers. The resulting ash plume is estimated to have been high. As gradually an unstable pulsating column formed, fed only by the most evolved magma due to upward migration of the fragmentation surface, reduced magma eruption rate, and/or activation of fractures, the Plinian phase ended. Emissions consisted of pumice and dark colored volcanic rock. The mafic minerals cover smaller areas than the more acidic members, also indicating a decrease of explosivity over the course of the eruption. The eruption column caused a large pumice-fall deposit to the east of the source area.
Pyroclastic density currents
The initial eruption was followed by a caldera collapse and a large pyroclastic flow, fed by the upper magma layer, a single flow unit with lateral variations in both pumice and lithic fragments, that covered an area of. Currents that moved toward the North and the South overflowed mountain ranges and crossed the Gulf of Naples over the sea, extinguishing all life within a radius of about. Textural and morphological features of the deposits, and areal distribution suggests that the eruption was of the type of highly expanded low-temperature pyroclastic cloud. The pyroclastic sequence from base to top:
densely welded ignimbrite and lithic-rich breccias
sintered ignimbrite, low-grade ignimbrite and lithic-rich breccia
lithic-rich breccia and spatter agglutinate
low-grade ignimbrite
Ignimbrite deposit
The ignimbrite is a gray, poorly to moderately welded, nearly saturated potassictrachyte, similar to many other trachytes of the Quaternary volcanic province of Campania. It consists of pumice and lithic fragments in a devitrified matrix that contains sanidine, lesser plagioclase rimmed by sanidine, two clinopyroxenes, biotite, and magnetite. The column collapse that generated the widespread ignimbrite deposit most likely occurred due to an increase of the Mass Eruption Rate ,. The immediate area was completely buried by thick layers of pyroclastic fragments, volcanic blocks, lapilli and ash. Two thirds of Campania sank under a layer of tuff as much as thick. The greater ignimbrite deposit, mostly trachytic ash and pumice, covered an area of at least, encompassing most of the southern Italian peninsula and the eastern Mediterranean region. Calculations of ash thickness measurements collected at 115 sites and a three dimensional ash dispersal model add up to a total amount of fallout material of 300 km3 of tephra across an area of. Considering volume estimations of up to for the proximal pyroclastic density current deposits, the total bulk volume of the CI eruption is covering most of the eastern Mediterranean and ash clouds reaching as far as central Russia.
Global impact
The event's recent dating at 39,280±110 years ago draws considerable scholarly attention as it marks a time interval characterized by biocultural modifications in western Eurasia and widespread discontinuities in archaeological sequences, such as the Middle to Upper Palaeolithic transition. At several archaeological sites of South-eastern Europe, the ash separates the cultural layers containing Middle Palaeolithic and/or Earliest Upper Palaeolithic assemblages from the layers in which Upper Palaeolithic industries occur. At some sites the CI tephra deposit coincides with a long interruption of paleo-human occupation.
Effect on climate
The climatic importance of the eruption was tested in a three-dimensional sectional aerosol model that simulated the global aerosol cloud under glacial conditions. Authors calculate that up to 450 million kilograms of sulphur dioxide would have been accumulated into the atmosphere, driving down temperatures at least by 1 to 2 degrees Celsius for a period of 2 to 3 years. The Heinrich event 4, the name given to a cooling period, characterized by a break off of unusual large sections of ice from polar glaciers occurred around 40,000 years ago being well documented in the North Atlantic Ocean, although its impact on terrestrial areas is a matter of ongoing debate.
Effect on living organisms
and chloride emissions caused acidic rains, fluorine-laden particles become incorporated into plant matter, potentially inducing dental fluorosis, replete with eye, lung and organ damage in animal populations.
The eruption coincided also with the final decline of the Neanderthal in Europe. Environmental stress caused by the eruption has been invoked as a potential explanation for the extinction as well as discontinuities in Palaeolithic societies, although the climatic effects of the eruption alone are considered insufficient to account for the demise of the Neanderthals in Europe. The notion remains contested; nonetheless, some studies suggest that significant volcanic cooling during the period immediately after the eruption might have severely disturbed these already precarious populations.
Island biodiversity
A joint study on the influence of the Late Quaternaryclimate change on island biodiversity has been published in 2016 in the Nature journal. This investigation on the consequences of abrupt climate changes for island biodiversity is apparently unprecedented. Established "island biogeographical models consider islands either as geologically static with biodiversity resulting from ecologically neutral immigration–extinction dynamics, or as geologically dynamic with biodiversity resulting from immigration–speciation–extinction dynamics influenced by changes in island characteristics over millions of years." Researchers argue that "climatic oscillations over short geological periods are likely to affect sea levels and cause huge changes in island size, isolation and connectivity, orders of magnitude faster than the geological processes of island formation..." Results suggest that "post-Last Glacial Maximum changes in island characteristics, especially in area, have left a strong imprint on the present diversity of endemic species."
Laschamp event
In 2012 the GFZ German Research Centre for Geosciences has published a study on likely causal connections between the Laschamp magnetic reversal and the eruption as "sediment cores from the Black Sea show that during this period a compass at the Black Sea would have pointed to the south instead of north." Evidence seems to be limited and the publication is no longer publicly available.
