The most recent understanding of the evolution of insects is based on studies of the following branches of science: molecular biology, insect morphology, paleontology, insect taxonomy, evolution, embryology, bioinformatics and scientific computing.
 It is estimated that the class of insects originated on Earth about 480 million years ago, in the Ordovician, at about the same time terrestrial plants appeared.
 Insects evolved from a group of crustaceans.
 The first insects were land bound, but about 400 million years ago in the Devonian period one lineage of insects evolved flight, the first animals to do so.
 The oldest definitive insect fossil, "Rhyniognatha hirsti", is estimated to be  396 .
 Global climate conditions changed several times during the history of Earth, and along with it the diversity of insects.
 The Pterygotes (winged insects) underwent a major radiation in the Carboniferous (356 to 299 million years ago) while the Endopterygota (insects that go through different life stages with metamorphosis) underwent another major radiation in the Permian (299 to 252 million years ago).
Before photosynthesis evolved, Earth's atmosphere had no free oxygen (O).
 Photosynthetic prokaryotic organisms that produced O as a waste product lived long before the first build-up of free oxygen in the atmosphere, perhaps as early as 3.5 billion years ago.
 The oxygen they produced would have been rapidly removed from the atmosphere by weathering of reducing minerals, most notably iron.
 This "mass rusting" led to the deposition of iron oxide on the ocean floor, forming banded iron formations.
 Oxygen only began to persist in the atmosphere in small quantities about 50 million years before the start of the Great Oxygenation Event.
 This mass oxygenation of the atmosphere resulted in rapid buildup of free oxygen.
 At current rates of primary production, today's concentration of oxygen could be produced by photosynthetic organisms in 2,000 years.
 In the absence of plants, the rate of oxygen production by photosynthesis was slower in the Precambrian, and the concentrations of O attained were less than 10% of today's and probably fluctuated greatly; oxygen may even have disappeared from the atmosphere again around 1.9 billion years ago.
 These fluctuations in oxygen concentration had little direct effect on life, with mass extinctions not observed until the appearance of complex life around the start of the Cambrian period,   million years ago .
 The presence of O2 provided life with new opportunities.
 Aerobic metabolism is more efficient than anaerobic pathways, and the presence of oxygen undoubtedly created new possibilities for life to explore.
 Since the start of the Cambrian period, atmospheric oxygen concentrations have fluctuated between 15% and 35% of atmospheric volume.
 The maximum of 35% was reached towards the end of the Carboniferous period (about 300 million years ago), a peak which may have contributed to the large size of insects and amphibians at that time.
 Whilst human activities, such as the burning of fossil fuels, affect relative carbon dioxide concentrations, their effect on the much larger concentration of oxygen is less significant.
In the geologic record the Chaotian eon or era is unofficially proposed to denote the time preceding the solidification of the Earth's crust and the formation of Earth's moon, it is the earliest era within the eon of Hadean.
 It lasted 196 million years, at   million years ago to the beginning of the Zirconian era,   million years ago .
 It is named after Chaos, the primeval void in Greek mythology.
 The Chaotian sets in with the emergence of Earth at 4.6 billion years ago.
 Its upper limit and thus the transition to the Zirconian era is defined by the occurrence of the first conservation capable mineral.
 These are zircon, the oldest mineral in the Jack Hills of Narryer Gneiss Terrane in Western Australia (Yilgarn craton) found and were dated 4,404 ± 8 million years ago
The Stiperstones is a distinctive hill in the county of Shropshire, England.
 It is a quartzite ridge.
 The quartzite rock formed some 480 million years ago.
 During the last Ice Age the summit stood out above the glaciers and was subject to constant freezing and thawing which shattered the quartzite into a mass of jumbled scree surrounding several residual rocky tors.
 At 536 m above sea level it is the second-highest hill in the county, surpassed only by Brown Clee Hill (540 m ).
 Stiperstones' 8 km summit ridge is crowned by several rugged, jagged outcrops of rock silhouetted against the sky.
The Appalachian Mountains ( , French: "les Appalaches" ), often called the Appalachians, are a system of mountains in eastern North America.
 The Appalachians first formed roughly 480 million years ago during the Ordovician Period.
 It once reached elevations similar to those of the Alps and the Rocky Mountains before naturally occurring erosion.
 The Appalachian chain is a barrier to east-west travel, as it forms a series of alternating ridgelines and valleys oriented in opposition to most roads running east or west.
Quaternary ( ) is the current and most recent of the three periods of the Cenozoic Era in the geologic time scale of the International Commission on Stratigraphy (ICS).
 It follows the Neogene Period and spans from 2.588 ± 0.005 million years ago to the present.
 The Quaternary Period is divided into two epochs: the Pleistocene (2.588 million years ago to 11.7 thousand years ago) and the Holocene (11.7 thousand years ago to today).
 The informal term "Late Quaternary" refers to the past 0.5–1.0 million years.
The evolution of fungi has been going on since fungi diverged from other life around 1.5 billion years ago, (Wang et al., 1999) with the glomaleans branching from the "higher fungi" at ~  million years ago , according to DNA analysis.
 (Schüssler et al., 2001; Tehler et al., 2000) Fungi probably colonized the land during the Cambrian, over   million years ago , (Taylor & Osborn, 1996) but terrestrial fossils only become uncontroversial and common during the Devonian,   million years ago .
The Cobequid Fault is a fault that is the extension of the Chedabucto Fault.
 This fault runs from Truro to Cape Chignecto south of the Cobequid Hills.
 Both the Cobequid fault and the Chedabucto Fault form the Minas Fault zone splitting Nova Scotia into the Avalon Zone and the Meguma Zone.
 Movement on the Cobequid Fault started before 400 million years ago and end around 40 million years ago.
 Between that time around 350 million years violent volcanic eruptions at Spicers Cove north Cape Chignecto Provincial Park and 50 million years after grey sandstone rich in fossil plants were deposited.
 At Five Islands Provincial Park there are red rocks formed by the large accumulation of mud, sand and gravel around 210 million years ago.
The Northern Appalachians Seismic Zone is an active seismic zone in the Appalachian Mountains of eastern North America, extending from New Brunswick southwards into New England and Boston.
 Both the seismic zone and the resultant Appalachian Mountains were created by the collision of two tectonic plates about 440–480 million years ago during the middle Ordovician Period.
The Trenton Prong is a physiographic subprovince of the Piedmont Uplands section of the Piedmont province of the Appalachian Mountains.
 The prong consists of crystalline metamorphic rock.

Question: The Trenton Prong is a section of the Piedmont province of what that was formed roughly 480 million years ago?
Answer: The Appalachian Mountains