FOSSIL FUELS AND THE EARTH'S MASS

A bright, beautiful young mind asked the question, "does Earth's mass decrease when we burn fossil fuels? And if it does, is it measurable? Do we know how much of the Earth’s mass has been lost so far?"

Well, Melaina, the Earth’s mass does decrease when fossil fuels are burnt. But not in the sense you were probably imagining, and only to a very, very small degree.

There is no decrease in chemical mass. Burning fossil fuels rearranges atoms into different molecules, in the process releasing energy from chemical bonds, but in the end, the same particles — protons, neutrons, and electrons — remain, so there is no decrease in mass there.

But energy is released, and some of that energy is radiated out into space, escaping from the Earth entirely. Einstein's Theory of Relativity tells us that energy does have mass: E=mc^2, or m=E/c^2. When a chemical bond that stores energy is formed, the resulting molecule has a very tiny bit more mass than the sum of the masses of the atoms from which it was formed, so a net gain. Wait, what?

Again, this is an exceedingly tiny bit. In very rough numbers, worldwide energy consumption is about 160,000 terawatt-hours per year, and about 80% of that comes from fossil fuels. That is about 450,000,000 TJ/year (tera-joules/year). The speed of light is 300,000,000 meter/s; dividing 450,000,000 TJ by (300,000,000 m/s)^2 gives a decrease in mass of 5000 kilograms per year.

That is an exceedingly small fraction — 50 billionths of one percent — of the approximately 10,000,000,000,000 kilograms of fossil fuels consumed per year. And as far as making the Earth lighter, it’s a tenth of a billionth of a billionth of a percent of the Earth’s mass.

Of course, the energy in fossil fuels originally came from the Sun, and in absorbing that sunlight the Earth’s mass increases slightly. I picture the Earth expanding and contracting, taking a deep breath, then exhaling. We don't see this when we look, but it is a great visual for imaging this never-ending give and take process. I'm not sure how we'd measure the small changes to the Earth's net mass on any given day. The mass of the Earth may be determined using Newton's law of gravitation. It is given as the force (F), which is equal to the Gravitational constant multiplied by the mass of the planet and the mass of the object, divided by the square of the radius of the planet.

Newton's insight on the inverse-square property of gravitational force was from an intuition about the motion of the earth and the moon. The mathematical formula for gravitational force is F=GMmr2 F = G Mm r 2 where G is the gravitational constant. I know, Newton’s law could use some curb appeal but it is super useful when understanding what keeps the Earth and other planets in our solar system in orbit around the Sun and why the Moon orbits the Earth. We have Newton to thank for his formulas on the gravitational potential of water when we build hydroelectricity dams. Newton’s ideas work in most but not all scenarios. When things get very, very small, or cosmic, gravity gets weird... and we head on back to Einstein to make sense of it all.

There was a very cool paper published yesterday by King Yan Fong et al. in the journal Nature that looked at heat transferring in a previously unknown way — heat transferred across a vacuum by phonons — tiny, atomic vibrations. The effect joins conduction, convection and radiation as ways for heating to occur — but only across tiny distances. The heat is transferred by phonons — the energy-carrying particles of acoustic waves, taking advantage of the Casimir effect, in which the quantum fluctuations in the space between two objects that are really, really close together result in physical effects not predicted by classical physics. This is another excellent example of the universe not playing by conventional rules when things get small. Weird, but very cool!

But the question was specifically about the mass of the Earth and the burning of fossil fuels, and that process does decrease the mass.

So it is mostly true that the Earth’s mass does not decrease due to fossil fuel burning because the numbers are so low, but not entirely true. The fuel combines with oxygen from the atmosphere to produce carbon dioxide, water vapour, and soot or ash. The carbon dioxide and water vapour go back into the atmosphere along with some of the soot or ash, the rest of which is left as a solid residue. The weight of the carbon dioxide plus the water vapour and soot is exactly the same as the weight of the original fuel plus the weight of the oxygen consumed. In general, the products of any chemical reaction whatsoever weigh the same as the reactants.

There is only one known mechanism by which Earth’s mass decreases to any significant degree: molecules of gas in the upper atmosphere (primarily hydrogen and helium, because they are the lightest) escape from Earth’s gravity at a steady rate due to thermal energy. This is counterbalanced by a steady rain of meteors hitting Earth from outer space (if you ever want to hunt them, fly a helicopter over the frozen arctic, they really stand out), containing mostly rock, water, and nickel-iron. These two processes are happening all the time and will continue at a steady rate unchanged by anything we humans do. So, the net/net is about the same.

So, the answer is that the Earth's mass is variable, subject to both gain and loss due to the accretion of in-falling material (micrometeorites and cosmic dust), and the loss of hydrogen and helium gas, respectively. But, drumroll please, the end result is a net loss of material, roughly 5.5×107 kg (5.4×104 long tons) per year.

The burning of fossil fuels has an impact on that equation, albeit a very small one, but an excellent question to ponder. A thank you and respectful nod to Les Niles and Michael McClennen for their insights and help with the energy consumption figures.

DOUVILLEICERAS MAMMILLATUM

Some lovely examples of Douvilleiceras mammillatum (Schlotheim, 1813), ammonites from the Lower Cretaceous (Middle-Lower Albian) Douvilliceras inequinodum zone of Ambarimaninga, Mahajanga Province, Madagascar.

The genus Douvilleiceras range from Middle to Late Cretaceous and can be found in Asia, Africa, Europe and North and South America. 

We have beautiful examples in the early to mid-Albian from the archipelago of Haida Gwaii in British Columbia. Joseph F. Whiteaves was the first to recognize the genus from Haida Gwaii when he was looking over the early collections of James Richardson and George Dawson. The beauties you see here measure 6cm to 10cm.

HOPLITES: TIRE-TRACK RIBBING

Hoplites Bennettiana, Troyes, France

An excellent example of the ammonite, Hoplites bennettiana (Sowby, 1826) with a pathology. This beauty is from Albian deposits near Carrière de Courcelles, Villemoyenne, laid down in the Cretaceous near la région de Troyes, Aube,  Champagne in northeastern France.

The Albian is the youngest or uppermost subdivision of the Lower Cretaceous, approximately 113.0 ± 1.0 Ma to 100.5 ± 0.9 Ma (million years ago).

L'Albien or Albian is both an age of the geologic timescale and a stage in the stratigraphic column. It was named after Alba, the Latin name for the River Aube, a tributary of the Seine that flows through the Champagne-Ardenne region of northwestern France.

At the time that this fellow was swimming in our oceans, ankylosaurs were strolling about Mongolia and stomping through the foliage in Utah, Kansas and Texas. Bony fish were swimming over what would become the strata making up Canada, the Czech Republic and Australia. Cartilaginous fish were prowling the western interior seaway of North America and a strange extinct herbivorous mammal, Eobaatar, was snuffling through Mongolia, Spain and England. 

Hoplites are amongst my favourite ammonites. I still have a difficult time telling them apart. To the right, you can see a slightly greyish, Hoplites maritimus, from Sussex England. 

Below him is a brownish Hoplites rudis from outcrops between Courcelles and Troyes, France. There are many Hoplites species. 

Each has the typical raised tire-track ribbing. My preference is for Hoplities bennetianus (or bennettiana). I'm still sorting out the naming of that species. The difference between Hoplites bennettiana and Hoplites dentatus is seen on the centre but I still find the distinctions subtle.

Hoplites shells have compressed, rectangular and trapezoidal whorl sections. They have pronounced umbilical bullae from which their prominent ribs branch out. The ends of the ribs can be both alternate or opposite. Some species have zigzagging ribs and these usually end thickened or raised into ventrolateral tubercles.

Photo One: Hoplites Bennettiana from near Troyes, France. Collection de Christophe Marot

Photo Two: Hoplites maritimus from Sussex, UK. Bottom: Hoplites rudis from near Troyes, France. Collection of Mark O'Dell

ABUNDANCE TO EXTINCTION: THE AMMONITES

Early Cretaceous Hoplites sp. Dorset, UK

Ammonites were predatory, squid-like creatures that lived inside coil-shaped shells. 

Like other cephalopods, ammonites had sharp, beak-like jaws inside a ring of tentacles that extended from their shells to snare prey such as small fish and crustaceans. Some ammonites grew more than three feet (one meter) across — possible snack food for the giant mosasaur Tylosaurus.

These sea creatures were constantly building new shell as they grew. Most ammonites have coiled shells. The chambered part of the shell is called a phragmocone.  It contains a series of progressively layered chambers called camerae, which were divided by thin walls called septae. The last chamber is the body chamber. Most of the shell was unused as they preferred to inhabit only the outer chamber. 

As the ammonite grew, it added new and larger chambers to the opened end of the shell. A thin living tube called a siphuncle passed through the septa, extending from the body to the empty shell chambers.

This allowed the ammonite to empty the water out of the shell chambers by hyperosmotic active transport process. This process controlled the buoyancy of the ammonite's shell. They scooted through the warm, shallow seas by squirting jets of water from their bodies. 

A thin, tubelike structure called a siphuncle reached into the interior chambers to pump and siphon air and helped them move through the water.

They first appeared about 240 million years ago, though they descended from straight-shelled cephalopods called bacrites that date all the way back to the Devonian — some 415 million years. 

They were prolific breeders, lived in schools, and are among the most abundant fossils found today. They went extinct with the dinosaurs 65 million years ago. Scientists use the various shapes and sizes of ammonite shells that appeared and disappeared through the ages to date other fossils.

During their evolution, three catastrophic events occurred. The first during the Permian period (250million years ago), only 10% survived.  They went on to flourish throughout the Triassic period, but at the end of this period (206 million years ago), all but one species died. Then they began to thrive from the Jurassic period until the end of the Cretaceous period when all species of ammonites became extinct.

Ammonites began life very tiny, less than 1mm in diameter, and were vulnerable to attack from predators. They fed on plankton and quickly assumed a strong protective outer shell. They also grew quickly with the females growing up to 400% larger than the males; because they needed the larger shell for egg production. Most ammonites only lived for two years.  Some lived longer becoming very large. The largest ever found was in Germany (6.5 feet in diameter).

Ammonites lived in shallow waters of 100 meters or less. They moved through the water by jet propulsion expelling water through a funnel-like opening to propel themselves in the opposite direction. They were predators (cephalopods) feeding on most living marine life including molluscs, fish even other cephalopods. Ammonites would silently stalk their prey then quickly extend their tentacles to grab it.  When caught the prey would be devoured by the Ammonites' jaws located at the base of the tentacles between the eyes.

Photo One: Hoplites sp. from the Early Cretaceous of Dorset, UK. Natural Selection Fossils

Photo Two: Hoplites dentalus from Albian deposits near Troyes, France. Collection of Stéphane Rolland.

Wright, C. W. (1996). Treatise on Invertebrate Paleontology, Part L, Mollusca 4: Cretaceous Ammonoidea (with contributions by JH Calloman (sic) and MK Howarth). Geological Survey of America and University of Kansas, Boulder, Colorado, and Lawrence, Kansas, 362.

Amédro, F., Matrion, B., Magniez-Jannin, F., & Touch, R. (2014). La limite Albien inférieur-Albien moyen dans l’Albien type de l’Aube (France): ammonites, foraminifères, séquences. Revue de Paléobiologie, 33(1), 159-279.

AVIAN RELATIONS

Although most of the skeletal features differentiating birds from other extant vertebrates can be traced back to the Mesozoic dinosaurs (Makovicky; Zanno, 2011; Xu et al., 2014a), the integration of the fossil record of stem-avians — all taxa closer to birds than crocodiles — with the developmental biology of living birds is more controversial.

The evolution of the three-fingered hand of birds from the ancestral pentadactyl condition of tetrapods is still debated, the former having been considered alternatively as homologous to the medial most three (I–II–III) or the central (II–III–IV) fingers of reptiles (Wagner & Gauthier, 1999; Bever, Gauthier & Wagner, 2011; Xu et al., 2014a).

This controversy has often been depicted as a dichotomy between a paleontological approach supporting the I–II–III pattern in three-fingered theropods, Tetanurans, and a developmental approach supporting the II–III–IV pattern based on the topology of the embryonic mesenchymal condensations from which the avian digits develop (Wagner & Gauthier, 1999).

Yet, both fossil and embryological data are involved in the two alternative interpretations (Bever, Gauthier & Wagner, 2011; Vargas et al., 2008; Xu et al., 2009; Tamura et al., 2011), and may eventually support additional, more complex, homology frameworks (Xu et al., 2014a). Pivotal among the fossil evidence, the unusual hand of the Late Jurassic ceratosaurian Limusaurus has been argued to support a II–III–IV digital identity in birds and a complex pattern of homeotic transformations in three-fingered, Tetanuran, theropods (Xu et al., 2009; Bever, Gauthier & Wagner, 2011), although criticism to this interpretation has been raised from both paleontological and developmental perspectives (Wang et al., 2011; Carrano & Choiniere, 2016).

Following the reinterpretation of the digital identity along the avian stem of Xu et al. (2009), a series of paleontological studies in the last decade used the II–III–IV homology pattern as a morphological framework for three-fingered theropods, challenging the I–II–III pattern traditionally followed in the interpretation of the theropod hand (Xu, Han & Zhao, 2014b). It must be remarked that the evolutionary scenario supporting the II–III–IV homology pattern of Xu et al. (2009) makes predictions that can be falsified in the fossil record (Bever, Gauthier & Wagner, 2011): the phalangeal formula at the root of Ceratosauria should be markedly simplified, compared to the ancestral theropod formula (i.e., 0-3-3/2-1-X vs 2-3-4-1-0).

The new ceratosaurian theropod, Saltriovenator zanellai, from the Saltrio Formation, Lower Jurassic, Lower Sinemurian, ∼198 million-year-old outcrops of Northern Italy (Dal Sasso, 2003), show a mosaic of features seen in four-fingered theropods and in basal tetanurans. Although fragmentary, the new theropod allows the reconstruction of the ancestral ceratosaurian hand, shedding light on the evolutionary digit pattern in tetanuran fingers and thus along the lineage leading to bird origin. The occurrence of large averostran theropods in the fossil record also helps us to understand the body size of this new Italian specimen and its stratigraphic and geochronological context.

The new find, in the context of Early Jurassic neotheropods Skeletal remains of theropod dinosaurs are extremely rare in the Lower Jurassic and most reports are of only fragmentary remains (Benton, Martill; Taylor, 1995; Owen, 1863; Woodward, 1908; Andrews, 1921; Cuny & Galton, 1993; Delsate & Ezcurra, 2014).

Ceratosaurian-grade taxa are absent until Middle Jurassic times (Maganuco et al., 2007; Pol & Rauhut, 2012), with one exception from the Pliensbachian–Toarcian of Northern Africa (Allain et al., 2007). This paucity of skeletal remains is a considerable gap in our knowledge of these animals at a time when theropods were diversifying rapidly. Just after the Triassic–Jurassic mass extinction event we begin to see a rich, worldwide distribution revealed through ichnofossils (Delsate & Ezcurra, 2014).

In Europe, we find theropod remains from the Hettangian, mostly non-diagnostic at the generic level: Scotland (Benton, Martill & Taylor, 1995), England (Owen, 1863; Woodward, 1908; Andrews, 1921), France (Cuny & Galton, 1993), and Luxembourg (Delsate & Ezcurra, 2014).

Two species of the genus Sarcosaurus have been reported from the Hettangian of England, S. woodi from Barrow upon Soar, Leicestershire, based on an isolated pelvis, vertebra, and proximal femur (BMNH 4840/1), and S. andrewsi (Huene, 1932), based on a partial tibia (NHMUK R3542) (Woodward, 1908).

There's also the neotheropod Dracoraptor hanigani, from the Hettangian of Wales, described by Martill et al. in 2016 on the basis of a 40% complete skeleton including cranial and postcranial material. In the rest of the world, the most famous Early Jurassic theropod is certainly Dilophosaurus wetherilli from the Hettangian of Arizona (Welles, 1954, 1984), which is known from several specimens.

Other relevant taxa are Sinosaurus (=“Dilophosaurus” sinensis) from the Hettangian–Sinemurian of China (Hu, 1993), Coelophysis rhodesiensis from the Hettangian–Pliensbachian of South Africa and Zimbabwe (Raath, 1990), a personal favourite Dracovenator from the Hettangian of South Africa (Yates, 2005), Cryolophosaurus from the Early Jurassic (?Sinemurian–Pliensbachian) of Antarctica (Hammer & Hickerson, 1994), Podokesaurus from the Pliensbachian to Toarcian of Massachusetts (Talbot, 1911), Segisaurus from the Pliensbachian to Toarcian of Arizona (Carrano, Hutchinson & Sampson, 2005), “Syntarsus” kayentakatae from the Hettangian of Arizona (Rowe, 1989), and Berberosaurus from the Toarcian of Morocco (Allain et al., 2007).

Ignored is the enigmatic genus Eshanosaurus from the Lower Jurassic of China, tentatively dated as Hettangian (Xu, Zhao & Clark, 2001), pending correct identification and reliably dating, as this purported therizinosaurian coelurosaur might just well be a sauropodomorph.

In this context, the discovery of the new specimen from the Sinemurian of Italy is extremely relevant as it is among the oldest Jurassic theropods, it is larger than all other pre-Aalenian theropods and it helps us to understand some of the macroevolutionary patterns that would have characterized the evolution of Theropoda during the Jurassic.

It also represents the first dinosaur skeleton from the Italian Alps, the first of Jurassic age, and the second theropod skeleton found in Italy after Scipionyx samniticus (Dal Sasso & Signore, 1998; Dal Sasso & Maganuco, 2011). The discovery of the specimen was described accidentally. For a more detailed account, see Dal Sasso, 2004 or the post here from March 9, 2020.

EVOLUTION OF FISH

The evolution of fish began about 530 million years ago with the first fish lineages belonged to the Agnatha, a superclass of jawless fish.

We still see them in our waters as cyclostomes but have lost the conodonts and ostracoderms to the annals of time. 

Like all vertebrates, fish have bilateral symmetry; when divided down the middle or central axis, each half is the same. Organisms with bilateral symmetry are generally more agile, making finding a mate, hunting or avoiding being hunted a whole lot easier. While we still find them on our menus, the ability to move quickly means they avoid being the snack of choice, an honour that falls more to the invertebrates with whom they share the sea.

When we envision fish, we generally picture large eyes, gills, a well-developed mouth. The earliest animals that we classify as fish appeared as soft-bodied chordates who lacked a true spine. While they were spineless, they did have notochords, a cartilaginous skeletal rod that gave them more dexterity than the cold-blooded invertebrates who shared those ancient seas and evolved without a backbone.

Fish would continue to evolve throughout the Paleozoic, diversifying into a wide range of forms. Several forms of Paleozoic fish developed external armour that protected them from predators. The first fish with jaws appeared in the Silurian period, after which many species, including sharks, became formidable marine predators rather than just the prey of arthropods.

Fishes in general respire using gills, are most often covered with bony scales and propel themselves using fins. There are two main types of fins, median fins and paired fins. The median fins include the caudal fin or tail fin, the dorsal fin, and the anal fin. Now there may be more than one dorsal, and one anal fin in some fishes.

The paired fins include the pectoral fins and the pelvic fins. And these paired fins are connected to, and supported by, pectoral and pelvic girdles, at the shoulder and hip; in the same way, our arms and legs are connected to and supported by, pectoral and pelvic girdles. This arrangement is something we inherited from the ancestors we share with fishes. They are homologous structures.

When we speak of early vertebrates, we're often talking about fishes. Fish is a term we use a lot in our everyday lives but taxonomically it is not all that useful. When we say, 'fish' we generally mean an ectothermic, aquatic vertebrate with gills and fins.

Rhacolepis Buccalis, an extinct genus of ray-finned fossil fish

Fortunately, many of our fishy friends have ended up in the fossil record. We may see some of the soft bits from time to time, as in the lovely Rhacolepis Buccalis, an extinct genus of ray-finned fossil fish in carbonate concretion from the Lower Cretaceous, Santana Formation, Brazil.

Not surprisingly, vertebrates with hard skeletons have a much better chance of being preserved than those with just soft parts and no teeth or bone to speak of.

In British Columbia, we have lovely two-dimensional Eohiodon rosei, a common freshwater fossil fish well-represented in Eocene deposits from the Allenby of Princeton and McAbee Fossil Beds near Cache Creek. We also have the Tiktaalik roseae, a large freshwater fish, from 375 million-year-old Devonian deposits on Ellesmere Island in Canada's Arctic. Tiktaalik is a wonderfully bizarre creature with a flat, almost reptilian head but also fins, scales and gills. We have other wonders from this time. There are also spectacular antiarch placoderms, Bothriolepsis, found in the Upper Devonian shales of Miguasha in Quebec.

There are fragments of bone-like tissues from as early as the Late Cambrian with the oldest fossils that are truly recognizable as fishes come from the Middle Ordovician from North America, South America and Australia. At the time, South America and Australia were part of a supercontinent called Gondwana. North America was part of another supercontinent called Laurentia and the two were separated by deep oceans.

Eohiodon rosei, McAbee Fossil Beds

These two supercontinents and others that were also present were partially covered by shallow equatorial seas and the continents themselves were barren and rocky. Land plants didn't evolve until later in the Silurian Period.

In these shallow equatorial seas, a large diverse and widespread group of armoured, jawless fishes evolved: the Pteraspidomorphi. The first of our three groups of ostracoderms. The Pteraspidomorphi are divided into three major groups: the Astraspida, Arandaspida and the Heterostraci.

The oldest and most primitive pteraspidomorphs were the Astraspida and the Arandaspida. You'll notice that all three of these taxon names contain 'aspid', which means shield. This is because these early fishes and many of the Pteraspidomorphi possessed large plates of dermal bone at the anterior end of their bodies. This dermal armour was very common in early vertebrates, but it was lost in their descendants.

Arandaspida is represented by two well-known genera: Sacabampaspis, from South America and Arandaspis from Australia. Arandaspis have large, simple, dorsal and ventral head shields. Their bodies were fusiform, which means they were shaped sort of like a spindle, fat in the middle and tapering at both ends. Picture a sausage that is a bit wider near the centre with a crisp outer shell.

DIPLOGRAPTUS

 

IDENTIFYING FOSSIL BONE

If you’re wondering if you have Fossil Bone, you’ll want to look for the telltale texture on the surface. It’s best to take the specimen outside & photograph it in natural light.

With fossil bone, you will be able to see the different canals and webbed structure of the bone, sure signs that the object was of biological origin.

As my good friend Mike Boyd notes, without going into the distinction between dermal bone and endochondral bone — which relates to how they form - or ossify — it's worth noting that bones such as the one illustrated here will usually have a layer of smooth (or periosteal) bone on the outer surface and spongy (or trabecular) bone inside.

The distinction can be seen in this photograph. The partial weathering away of the smooth external bone has resulted in the exposure of the spongy bone interiors. Geographic context is important, so knowing where it was found is very helpful for an ID. 

Knowing the geologic context of your find can help you to figure out if you've perhaps found a terrestrial or marine fossil. Did you find any other fossils nearby? Can you see pieces of fossil shells or remnants of fossil leaves? Things get tricky with erratics. That's when something has deposited a rock or fossil far from the place it originated. We see this with glaciers. The ice can act like a plough, lifting up and pushing a rock to a new location, then melting away to leave something out of context.

TRENT RIVER PALAEONTOLOGY

Trent River, Vancouver Island, BC

The rocks that make up the Trent River on Vancouver Island were laid down south of the equator as small, tropical islands. They rode across the Pacific heading north and slightly east over the past 85 million years to where we find them today.

The Pacific Plate is an oceanic tectonic plate that lies beneath the Pacific Ocean. And it is massive. At 103 million km2 (40 million sq mi), it is the largest tectonic plate and continues to grow fed by volcanic eruptions that piggyback onto its trailing edge.

This relentless expansion pushes the Pacific Plate into the North American Plate. The pressure subducts it beneath our continent where it then melts back into the earth. Plate tectonics are slow but powerful forces. 

The island chains that rode the plates across the Pacific smashed into our coastline and slowly built the province of British Columbia. And because each of those islands had a different origin, they create pockets of interesting and diverse geology.

It is these islands that make up the Insular Belt — a physio-geological region on the northwestern North American coast. It consists of three major island groups — and many smaller islands — that stretches from southern British Columbia up into Alaska and the Yukon. These bits of islands on the move arrived from the Late Cretaceous through the Eocene — and continues to this day.

The rocks that form the Insular Superterrane are allochthonous, meaning they are not related to the rest of the North American continent. The rocks we walk over along the Trent River are distinct from those we find throughout the rest of Vancouver Island, Haida Gwaii, the rest of the province of British Columbia and completely foreign to those we find next door in Alberta.

To discover what we do find on the Trent takes only a wee stroll, a bit of digging and time to put all the pieces of the puzzle together. The first geological forays to Vancouver Island were to look for coal deposits, the profitable remains of ancient forests that could be burned to power industry.

Jim Monger and Charlie Ross of the Geological Survey of Canada both worked to further our knowledge of the complex geology of the Comox Basin. They were at the cutting edge of west coast geology in the 1970s. It was their work that helped tease out how and where the rocks we see along the Trent today were formed and made their way north.

We know from their work that by 85 million years ago, the Insular Superterrane had made its way to what is now British Columbia. The lands were forested much as they are now but by extinct genera and families. The fossil remains of trees similar to oak, poplar, maple and ash can be found along the Trent and Vancouver Island. We also see the lovely remains of flowering plants such as Cupanities crenularis, figs and breadfruit.

Heading up the river, you come to a delineation zone that clearly marks the contact between the dark grey marine shales and mudstones of the Haslam Formation where they meet the sandstones of the Comox Formation. Fossilized material is less abundant in the Comox sandstones but still contains some interesting specimens. Here you begin to see fossilized wood and identifiable fossil plant material.

Further upstream, there is a small tributary, Idle Creek, where you can find more of this terrestrial material in the sandy shales. As you walk up, you see identifiable fossil plants beneath your feet and jungle-like, overgrown moss-covered, snarly trees all around you.

Polyptychoceras vancouverense / BCPA 2003

Walking west from the Trent River Falls at the bottom, you pass the infamous Ammonite Alley, where you can find Mesopuzosia sp. and Kitchinites sp. of the Upper Cretaceous (Santonian), Haslam Formation. Minding the slippery green algae covering some of the river rocks, you can see the first of the Polytychoceras vancouverense zone.

Continuing west, you reach the first of two fossil turtle sites on the river — amazingly, one terrestrial and one marine. If you continue, you come to the Inland Island Highway.

The Trent River has yielded some very interesting marine specimens, and significant terrestrial finds. We've found both a wonderful terrestrial helochelydrid turtle, Naomichelys speciosa, and the caudal vertebrae of a Hadrosauroid dinosaur. Walking down from the Hadrosaur site you come to the site of the fossil ratfish find — one of the ocean's oddest fish.

Ratfish, Hydrolagus Collie, are chimaera found in the north-eastern Pacific Ocean today. The fossil specimen from the Trent would be considered large by modern standards as it is a bruiser in comparison to his modern counterparts. This robust fellow had exceptionally-large eyes and sex organs that dangled enticingly between them. You mock, but there are many ratfish who would differ. While inherently sexy by ratfish standards, this fellow was not particularly tasty to their ancient marine brethren (or humans today) — so not hugely sought after as a food source or prey.

A little further again from the ratfish site we reach the contact of the two Formations. The rocks here have travelled a long way to their current location. With them, we peel away the layers of the geologic history of both the Comox Valley and the province of British Columbia.

Photo One: Trent River, Haslam Formation, Fossil Huntress. Photo Two: Polyptychoceras vancouverense from the Upper Cretaceous (Santonian), Haslam formation, Trent River, Vancouver Island, British Columbia, Canada. 2003 BCPA Calendar.

References: Note on the occurrence of the marine turtle Desmatochelys (Reptilia: Chelonioidea) from the Upper Cretaceous of Vancouver Island Elizabeth L. Nicholls Canadian Journal of Earth Sciences (1992) 29 (2): 377–380. https://doi.org/10.1139/e92-033; References: Chimaeras - The Neglected Chondrichthyans". Elasmo-research.org. Retrieved 2017-07-01.

Directions: If you're keen to explore the area, park on the side of Highway 19 about three kilometres south of Courtenay and hike up to the Trent River. Begin to look for parking about three kilometres south of the Cumberland Interchange. There is a trail that leads from the highway down beneath the bridge which will bring you to the Trent River's north side.

UNEARTHING A JUVENILE ELASMOSAUR ON THE TRENT RIVER

Pat Trask with a Fossil Rib Bone. Photo: Rebecca Miller

A mighty marine reptile was excavated on the Trent River near Courtenay on the east coast of Vancouver Island, British Columbia, Canada in August 2020.

The excavation is the culmination of a three-year palaeontological puzzle.

The fossil remains are those of an elasmosaur — a group of long-necked marine reptiles found in the Late Triassic to the Late Cretaceous some 215 to 80 million years ago. 

In the case of the Trent River, it is closer to 85 million years old. The rocks that make up this riverbed today were laid down south of the equator as small, tropical islands. They rode slow-moving tectonic plates across the Pacific — heading north and slightly east over the past 85 million years to where we find them today.

The marine reptile fossil was excavated 10-meters up high on the cliffs that line the river. It took a month of careful planning, building scaffolding, and amassing climbing gear to aid the team of dedicated souls in unearthing this juvenile elasmosaur. 

Bits and pieces of him have been eroding out for years — providing clues to the past and a jigsaw puzzle that has finally had the last pieces put together. The first piece of this marine reptile puzzle was found three years ago. 

The Courtenay Museum hosts regular fossil tours here, led by Pat Trask. On one of those field trips back in 2017, Pat was leading a trip with a family and one of the field trip participants picked up a marine reptile finger bone. It was laying in the river having eroded out from a nearby cliff. She showed it to Pat and he immediately recognized it as being diagnostic — it definitely belonged to a marine reptile — possibly an elasmosaur — but what species and just where on the river it had eroded from were still a mystery. She kindly donated it to the museum and that was that.

While it was an exciting find, it was a find without origin. Just where the material was coming from was unknown. It could have eroded from anywhere upstream and while many had searched the river, no other bone bits were found.   

Pat Trask Wrapping the plaster casing

Then in 2018, another piece of this paleontological puzzle was revealed. Pat was leading yet another Courtenay Museum Fossil Tour on the Trent River when one of the participants showed him a specimen that looked like a really tiny hockey puck. This second find was a wrist bone — again possibly from an elasmosaur but hard to be sure. Contemplating out loud where this material could be coming from, Pat looked down and found a vertebra in the water below his feet.

Pat put the bones in the lab at the museum. Intrigued by their origin, he began heading down to the river on his off hours to see where they might be coming from and thinking about where the erosion occurs on the Trent. 

In 2019, "I came down here and I started thinking about where the water flow would go." He could see a ledge along the river where eroded material might gather. Once he checked, he found a crack and cleaned out all the rock gathered there, finding more than a dozen bones. Pat teamed up with members of the Vancouver Island Palaeontological Society (VIPS) to scale the cliff faces above that section of the river. Jason Hawley, VIPS, did some rappelling but missed the site by a matter of feet.  

Pat had his neighbour fly a drone along the cliff face but it, too, turned up with nothing. Then at the beginning of August, Pat was back on the river in the morning with a family and said to one of the kids, "Hey, let's go look for baby elasmosaur." then they walked right over and saw a neckbone or tailbone in the river. Pat knew it hadn't been there the day before. He looked up and thought it must be coming from right up here. He came back later in the day with Deb Griffiths, his wife, set up his telescope on the river aimed at the likely portion of the cliff and bingo — he could see a bone sticking out.

He returned the next day with his brother Mike Trask. Mike found the elasmosaur on the Puntledge River back in 1988.  "We took a long pole and I said here's my target — and I hit one little piece, maybe three inches by three inches. When it fell down it had bones in it." Excited, they began planning a larger excavation that would include scaffolding, safety planning, climbing gear, permits... a lot of work in a short time. 

Plesiosaur Gastrolith

Initially, they thought there would be a small amount of fossil material, perhaps a few finger bones but over the past few weeks, they have found bones of at least half a marine reptile. 

And the beauty of this find is that most of the bones do not have to be prepared. They are literally eroding out of the matrix. No prep means no tools. Tools can impact the shape of a bone as you prepare it. They've found the pelvis bones, humerus, radius — all diagnostic to identify the genus. And this may be a new species. If it is, there is a good chance it will be named after the Trask family. 

I caught up with Pat and the team from the VIPS out on the river on August 23, 2020 — the day of the excavation. Loose rib bones, gastroliths, wrist bones, finger bones and part of the back and pelvis were recovered — and possibly the head, too. 

The bulk of the specimen was wrapped in plaster and carefully lowered to the ground by Pat and members of the VIPS, under Mike Trask's careful eye. We know that there is a femur in that jacket and possibly all the bones associated with that. Also included are the fibula and tibia and their associated bones — and I'm truly hoping there is a skull in there, too! I've popped a link below of a wee video showing the final moments as the plaster cast is lowered down from the excavation site. Take a look! It was quite an exciting moment.

It is not quite a baby, but this diminutive fellow is about four-metres long, making it a juvenile of his species. We have prepped enough of the material now to safely call it an elasmosaur. James Wood of the VIPS has done an amazing job on the preparation of this specimen using a new smaller air abrasive purchased by the Courtenay Museum. 

I hope to see it published with the Trask family name. Their paleontological history is forever tied to the Comox Valley and the honour would be fitting.  

Photo One: Rebecca Miller, Little Prints Photography — she is awesome!

Photo Two: James Wood prepped the material and Pat Trask labelled and oriented the bones.

Photo Three: Pat Trask perched atop scaffolding along the Trent River. And yes, he's attached to a safety line to secure him in case of fall. 

Photo Four: A gastrolith recovered amongst the stomach contents of the Trent River excavation. A gastrolith is a rock held inside a gastrointestinal tract. Gastroliths in some species are retained in the muscular gizzard and used to grind food in animals lacking suitable grinding teeth. The grain size depends upon the size of the animal and the gastrolith's role in digestion. Other species, including marine reptiles, use gastroliths as ballast — which may have been the case here. 

See the Excavation Moment via Video Link: https://youtu.be/r82EcEF7Pfc

UPPER CRETACEOUS FAUNA OF THE PACIFIC

Mosasaur from Manitoba, Courtenay Museum Collection

The Pacific fauna from the Upper Haslam Formation was cut-off geographically from their contemporaries living in the waters of the Western Interior Seaway.

That Seaway — also called the Cretaceous Seaway, the Niobrara Sea, the North American Inland Sea, and the Western Interior Sea  — was the large inland sea that formed during the mid- to late Cretaceous and again during the very early Paleogene. 

It split the continent of North America into two landmasses, Laramidia to the west and Appalachia to the east. We see evidence of this isolation when we look at the fossil marine reptiles from the Late Cretaceous Nanaimo Group of Vancouver Island. The Late Cretaceous Western Interior Seaway of North America has an abundant and well-studied record of fossil marine reptiles. The Pacific faunas we find on Vancouver Island were isolated from their contemporaneous faunas in the Western Interior Seaway. The ancient sea stretched from the Gulf of Mexico and through the middle of the modern-day countries of the United States and Canada, meeting with the Arctic Ocean to the north. At its largest, it was 2,500 feet (760 m) deep, 600 miles (970 km) wide and over 2,000 miles (3,200 km) long.

Betsy Nicholls and Dirk Meckert published on the marine reptiles from the Nanaimo Group (Upper Cretaceous) of Vancouver Island in the Canadian Journal of Earth Sciences in 2002.

They were comparing the newly discovered fossil from the Haslam and Pender formations (upper Santonian) near Courtenay, British Columbia, which include elasmosaurid plesiosaurs, turtles, and mosasaurs. These finds are only the second fauna of Late Cretaceous marine reptiles known from the Pacific Coast, the other being the fossiliferous shales from the Chico Group, Moreno Formation of California (Maastrichtian) that overlies the Panoche Formation.

The Nanaimo Group fossils are some 15 million years older than those from the Moreno Formation. Similarly to the California fauna, there are no polycotylid plesiosaurs — though the Nanaimo Group fauna does include a new genus of mosasaur. The species that we find on Vancouver Island lived at the same time but were not mixing geographically. What we see in our faunal mix reinforces the provinciality of the Pacific faunas and their isolation from contemporaneous faunas in the Western Interior Seaway.

Elizabeth L Nicholls and Dirk Meckert; Marine reptiles from the Nanaimo Group (Upper Cretaceous) of Vancouver Island; Canadian Journal of Earth Sciences, 2002, 39(11): 1591-1603, https://doi.org/10.1139/e02-075

TURTLE SHELLS AND DERMAL PLATES

Turtle shells are different from the body armour or armoured shells we see adorning dinosaurs like the ankylosaurs. These bad boys were blessed with huge plates of bone embedded into their skin that acted as a natural shield against predators. 

We find similar body armour is found on a crocodile or armadillo.

Turtles are covered by a special bony or cartilaginous shell that originates in their ribs. It is a useful adaptation to help deter predators as their soft interior makes for a tasty snack. 

Though I've never eaten turtle, it was a common and sought after meat for turtle soup. I'd read of Charles Darwin craving it after trying it for the first time on his trip in 1831 aboard the HMS Beagle. It seems Charlie like to taste every exotic new species he had the opportunity to try.

Turtle armour is made of dermal bone and endochondral bones from their vertebrae and rib cage. It is fundamentally different from the armour seen on our other vertebrate friends and the design creates some unique features in turtles. Because turtle ribs fuse together with some of their vertebrae, they have to pump air in and out of the lungs with their leg muscles. 

Another unusual feature in turtles is their limb girdles (pectoral and pelvic) have come to lie 'within' their rib cage, a feature that allows some turtles to pull their limbs inside the shell for protection. Sea turtles didn't develop this behaviour (or ability) and do not retract into their shells like other turtles.

Armadillos have armour formed by plates of dermal bone covered in relatively small, overlapping epidermal scales called scutes, composed of bone with a covering of horn. In crocodiles, their exoskeletons form their armour, similar to ankylosaurs. A bit of genius design, really. It is made of protective dermal and epidermal components that begin as rete Malpighii: a single layer of short, cylindrical cells that lose their nuclei over time as they transform into a horny layer.

Depending on the species and age of the turtle, turtles eat all kinds of food including seagrass, seaweed, crabs, jellyfish, and shrimp,. That tasty diet shows up in the composition of their armour as they have oodles of great nutrients to work with. The lovely example you see here is from the Oxford Museum collections.

GREEN SEA TURTLE

The Green Sea Turtle, Chelonia mydas, also known as the Green Turtle, Black Sea Turtle or Pacific Green Turtle is a species in the family Cheloniidae.

It is the only species in the genus Chelonia. Its range extends throughout tropical and subtropical seas around the world, with two distinct populations in the Atlantic and Pacific Oceans, but it is also found in the Indian Ocean. The common name refers to the usually green fat found beneath its carapace, not to the colour of its carapace, which is olive to black.

This sea turtle's dorsoventrally flattened body is covered by a large, teardrop-shaped carapace; it has a pair of large, paddle-like flippers. It is usually lightly coloured, although in the eastern Pacific populations' parts of the carapace can be almost black. Unlike other members of its family, such as the hawksbill sea turtle, C. mydas is mostly herbivorous. The adults usually inhabit shallow lagoons, feeding mostly on various species of seagrasses. The turtles bite off the tips of the blades of seagrass, which keeps the grass healthy.

Like other sea turtles, green sea turtles migrate long distances between feeding grounds and hatching beaches. Many islands worldwide are known as Turtle Island due to green sea turtles nesting on their beaches. Females crawl out on beaches, dig nests and lay eggs during the night. Later, hatchlings emerge and scramble into the water. Those that reach maturity may live to 80 years in the wild.

Researchers at the Senckenberg Research Institute in Frankfurt, Germany discovered the remains of the oldest fossilized sea turtle known to date. Remains from a new species, Desmatochelys padillai sp, including fossilized shell and bones have been found at two outcrops near Villa de Leyva, Colombia. The find was published in the journal PaleoBios, dates the reptile at 120 million years old – 25 million years older than any previously known specimen of this beautiful and long-lived turtle.

A TASTE FOR STUDIES

Green Sea Turtle, Chelonia mydas

While eating study specimens is not in vogue today, it was once common practice for researchers in the 1700-1880s. Charles Darwin belonged to a club dedicated to tasting exotic meats, and in his first book wrote almost three times as much about dishes like armadillo and tortoise urine than he did on the biogeography of his Galapagos finches.

One of the most famously strange scientific meals occurred on January 13, 1951, at the 47th Explorers Club Annual Dinner (ECAD) when members purportedly dined on a frozen woolly mammoth. The prehistoric meat was supposedly found on Akutan Island in Alaska, USA, by the eminent polar explorers' Father Bernard Rosecrans Hubbard, “the Glacier Priest,” and Captain George Francis Kosco of the US Navy.

This much-publicized meal captured the public’s imagination and became an enduring legend and source of pride for the Club, popularizing an annual menu of “exotics” that continues today, making the Club as well-known for its notorious hors d’oeuvres like fried tarantulas and goat eyeballs as it is for its notable members such as Teddy Roosevelt and Neil Armstrong.

The Yale Peabody Museum holds a sample of meat preserved from the 1951 meal, interestingly labeled as a South American Giant Ground Sloth, Megatherium, not Mammoth. The specimen of meat from that famous meal was originally designated BRCM 16925 before a transfer in 2001 from the Bruce Museum to the Yale Peabody Museum of Natural History (New Haven, CT, USA) where it gained the number YPM MAM 14399.

The specimen is now permanently deposited in the Yale Peabody Museum with the designation YPM HERR 19475 and is accessible to outside researchers. The meat was never fixed in formalin and was initially stored in isopropyl alcohol before being transferred to ethanol when it arrived at the Peabody Museum. DNA extraction occurred at Yale University in a clean room with equipment reserved exclusively for aDNA analyses.

In 2016, Jessica Glass and her colleagues sequenced a fragment of the mitochondrial cytochrome-b gene and studied archival material to verify its identity, which if genuine, would extend the range of Megatherium over 600% and alter views on ground sloth evolution. Their results showed that the meat was not Mammoth or Megatherium, but a bit of Green Sea Turtle, Chelonia mydas. So much for elaborate legends. The prehistoric dinner was likely meant as a publicity stunt. Glass's study emphasizes the value of museums collecting and curating voucher specimens, particularly those used for evidence of extraordinary claims. Not so long before Glass et al. did their experiment, a friend's mother (and my kayaking partners) served up a steak from her freezer to dinner guests in Castlegar that hailed from 1978. Tough? Inedible? I have it on good report that the meat was surprisingly divine.

Reference: Glass, J. R., Davis, M., Walsh, T. J., Sargis, E. J., & Caccone, A. (2016). Was Frozen Mammoth or Giant Ground Sloth Served for Dinner at The Explorers Club?. PloS one, 11(2), e0146825. https://doi.org/10.1371/journal.pone.0146825
at 17:48 

STUPENDEMYS GEOGRAPHICUS: A COLOSSAL TURTLE

Freshwater turtles come in all shapes and sizes but one of the most interesting and massive of these is the now-extinct freshwater turtle Stupendemys geographicus.

These aquatic beasties had shells almost three metres long (up to 9.5 feet) making it about a 100 times larger and sharing mixed traits with some of it's nearest living relatives — the giant South American River Turtle, Podocnemis expansa and Yellow-Spotted Amazon River Turtle, Podocnemis unifilis, the Amazon river turtle, Peltocephalus dumerilianus, and twice that of the largest marine turtle, the leatherback, Dermochelys coriacea.

It was also larger than those huge Archelon turtles that lumbered along during the Late Cretaceous at a whopping 15 feet, just over 4.5 metres. Stupendemys geographicus lived during the Miocene in Venezuela and Columbia. South America is a treasure trove of unique fossil fauna.

Throughout its history, the region has been home to giant rodents and an amazing assortment of crocodylians. It was also home to one of the largest turtles that ever lived. But for many years, the biology and systematics of Stupendemys geographicus remained largely unknown. When we found them in the fossil record it is usually as bits and pieces of shell and bone; exciting finds but not enough for us to see the big picture.

Palaeontologist Rodolfo Sánchez with Stupendemys geographicus

Back in 1994, several new shells and the first lower jaws of Stupendemys were found in the Urumaco region near Falcón State, Venezuela. The area is known to palaeontologists as a hotbed rich in well-preserved fossils. Fossil specimens of Stupendemys geographicus were first found here back in the 1970s by Harvard University researchers.

But for almost four decades, very few complete carapaces or other telltale fossils of Stupendemys were found in the region.

This excited Edwin Cadena, Paleontologist at the Universidad del Rosario in Colombia and researchers of the University of Zurich (UZH) and fellow researchers from Colombia, Venezuela, and Brazil. They had very good reason to believe that it was just a matter of time before more complete specimens were to be found. The area is a wonderful place to do fieldwork. It's an arid, desert locality without plant or forest coverage we see at other sites. Fossils weather out but do not wash away like they do at other sites.

Their efforts paid off and the fossils are marvellous. Shown here is Venezuelan Palaeontologist Rodolfo Sánchez with a male carapace (showing the horns) of Stupendemys geographical. This is one of the 8 million-year-old specimens from Venezuela.

Rodolfo Sánchez with Stupendemys geographicus

The team collected the most recent finds from Urumaco and added them fossil specimens from La Tatacoa Desert in Colombia.

Together, they paint a much clearer picture of a large terrestrial turtle that varied its diet and had distinct differences between the males and females in their morphology. Cadena published in February of this year with his colleagues in the journal Science Advances.

The researchers grouped together from multiple sites to help create a better understanding of the biology, lifestyle and phylogenetic position of these gigantic neotropical turtles.

Their paper includes the reporting of the largest carapace ever recovered and argues for a sole giant erymnochelyin taxon, S. geographicus, with extensive geographical distribution in what was the Pebas and Acre systems — pan-Amazonia during the middle Miocene to late Miocene in northern South America).

This turtle was quite the beast with two lance-like horns and battle scars to show it could hold its own with the apex predators of the day.

They also hypothesize that S. geographicus exhibited sexual dimorphism in shell morphology, with horns in males and hornless females. From the carapace length of 2.40 metres, they estimate to total mass of these turtles to be up to 1.145 kg, almost 100 times the size of its closest living relative. The newly found fossil specimens greatly expand the size of these fellows and our understanding of their biology and place in the geologic record.

Their conclusions paint a picture of a single giant turtle species across the northern Neotropics, but with two shell morphotypes, further evidence of sexual dimorphism. These were tuff turtles to prey upon. Bite marks and punctured bones tell us that they faired well from what must have been frequent predatory interactions with large, 30 foot long (over 9 metres) Caimans — big, burly alligatorid crocodilians — that also inhabited the northern Neotropics and shared their roaming grounds. Even with their large size, they were a very tempting snack for these brutes but unrequited as it appears Stupendemys fought, won and lumbered away.

Image Two: Venezuelan Palaeontologist Rodolfo Sánchez and a male carapace of Stupendemys geographicus, from Venezuela, found in 8 million years old deposits. Photo credit: Jorge Carrillo

Image Three: Venezuelan Palaeontologist Rodolfo Sánchez and a male carapace of Stupendemys geographicus, from Venezuela, found in 8 million years old deposits. Photo credit: Edwin Cadena

Reference: E-A. Cadena, T. M. Scheyer, J. D. Carrillo-Briceño, R. Sánchez, O. A Aguilera-Socorro, A. Vanegas, M. Pardo, D. M. Hansen, M. R. Sánchez-Villagra. The anatomy, paleobiology and evolutionary relationships of the largest side-necked extinct turtle. Science Advances. 12 February 2020. DOI: 10.1126/sciadv.aay4593

ICHY OF THE HUMBOLDT MOUNTAINS

A very well preserved ichthyosaur block with three distinct vertebrae and some ribs just peeking out. You can see the edges of the ribs nicely outlined against the matrix.

Ichthyosaurs are an extinct order of marine reptiles from the Mesozoic era. They evolved from land-dwelling, lung-breathing reptiles, they returned to our ancient seas and evolved into the fish-shaped creatures we find in the fossil record today.

They were visibly dolphin-like in appearance but seem to share some other qualities as well. These lovelies were warm-blooded and used their colouration as camouflage. The smaller of their lineage to avoid being eaten and the larger to avoid being seen by prey. Ichthyosaurs also had insulating blubber, a lovely adaptation to keep them warm in cold seas.

Over time, their limbs fully transformed into flippers, sometimes containing a very large number of digits and phalanges. Their flippers tell us they were entirely aquatic as they were not well-designed for use on land. And it was their flippers that first gave us the clue that they gave birth to live young; a hypothesis later confirmed by fossil embryo and wee baby ichy specimens.

We find their fossil remains in outcrops spanning from the mid-Cretaceous to the earliest Triassic. As we look through the fossils, we see a slow evolution in body design moving towards that enjoyed by dolphins and tuna by the Upper Triassic, albeit with a narrower, more pointed snout. 

During the early Triassic period, ichthyosaurs evolved from a group of unidentified land reptiles that returned to the sea. They were particularly abundant in the later Triassic and early Jurassic periods before being replaced as a premier aquatic predator by another marine reptilian group, the Plesiosauria, in the later Jurassic and Cretaceous periods. The block you see here is from Middle Triassic (Anisian/Ladinian) outcrops in the West Humboldt Mountains, Nevada.

MAPPING THE TRIASSIC: TOZER AND SILBERLING

In the early 1980s, Canadian palaeontologist Tim Tozer of the Geological Survey of Canada took a good long look at the marine invertebrate fauna in the Triassic of North America. 

Born in Britain and lost to us in December of 2011, at the age of 82. He was a colleague, friend and mentor. Tozer explored and mapped much of the high Arctic — one of the most remote and inhospitable areas of our planet. The work suited his rugged nature and natural curiosity. 

He loved to learn, solve puzzles and share his knowledge and enthusiasm with colleagues. His vast knowledge of the Triassic — both the biostratigraphy and ammonite taxonomy gained through lived experience — will never be repeated.  

Tozer mapped much of the Arctic Archipelago and was a renowned expert on the Triassic — our world 250 to 200 million years ago. He had a particular fondness for ammonoids, our cephie friends who reveal so much of our ancient past to us. Over his forty-plus year career, Tozer named and published on more than 200 species of Triassic ammonoids. 

Tozer collaborated with the American palaeontologist Norman J. Silberling, to define stratotypes for all the recognized North American biozones. Their North American zonal scheme is now accepted as the standard for Triassic global biostratigraphy and allows Alpine (western Tethyan) and Boreal (Siberian) zones to be placed in their proper chronological sequence.

Isolated occurrences of marine Triassic rocks in western North America were known by 1890, but discoveries of several hundred new localities from the Western Canada Sedimentary Basin and the Sverdrup Basin of Arctic Canada between about 1955 and 1980 added much information to the biochronology of the region. It also was recognized that more than half the world’s known genera of ammonoids occurred in North America, testifying to the cosmopolitan nature of the group. 

Tim Tozer, GSC, Mapping the Arctic Archipelago

Unhappy with the challenges of using the Alpine succession as a standard for the Triassic, Tozer and Silberling proposed their new zonal scheme based on relatively complete and in-place sequences in Arctic Canada, northeastern British Columbia, and the western United States.

Because of the endemism — restriction in the geographic distribution — of most ammonoid species, it is often difficult to correlate faunal assemblages between widely separated regions. Because ammonoids and conodonts are found together, a conodont biochronology can often be accurately intercalibrated with the ammonoid zonation, as established for North America by Michael (Mike) Orchard, from the Geologic Survey of Canada (GSC), Vancouver branch, whom Tozer mentored when Mike first joined the GSC as a post-doc.

Additional tools for correlation include the development of a Triassic sea-level curve for the Sverdrup Basin of Arctic Canada and a Triassic magnetic polarity timescale derived from paleomagnetic studies of mainly sedimentary sequences. Correlating rocks by means of polarity time units imprinted on rocks at the time they form is known as magnetochronostratigraphy and is likely to become more important in the future.

In the western terranes of the Cordillera, marine faunas from southern Alaska and Yukon to Mexico are known from the parts that are obviously allochthonous with regard to the North American plates.

Lower and upper Triadic faunas of these areas, as well as some that are today up to 63 ° North, have the characteristics of the lower paleo latitudes. 

In the western Cordillera, these faunas of the lower paleo latitudes can be found up to 3,000 km north of their counterparts on the American plate. This indicates a tectonic shift of significant magnitude. There are marine triads on the North American plate over 46 latitudes from California to Ellesmere Island. For some periods, two to three different faunal provinces can be distinguished. The differences infaunal species are linked, not surprisingly, to their paleolatitude. They are called LPL, MPL, HPL (lower, middle, higher paleolatitude).

I had the opportunity to head to Nevada last year to look at the Triassic ammonoids and ichthyosaur remains in the West Humboldt Mountains. Nevada provides the diagnostic features of the lower (LPL); northeastern British Columbia that of the middle (MPL) and Sverdrup Basin, the large igneous province on Axel Heiberg Island and Ellesmere Island, Nunavut, Canada near the rifted margin of the Arctic Ocean, that of the higher paleolatitude (HPL).

A distinction between the provinces of the middle and the higher paleo-situations can not be made for the lower Triassic and lower Middle Triassic (anise). However, all three provinces can be seen in the deposits of Ladin, Kam and Nor.

In the early 2000s, as part of a series of joint UBC, VIPS and VanPS fossil field trips (and then Chair of the VanPS), I explored much of the lower faunal outcrops of northeastern British Columbia. It was my first time seeing many of British Columbia's Triassic outcrops. The Nevada faunal assemblages are a lovely match. The quality of preservation at localities like Fossil Hill in the Humboldt Mountains of Nevada, perhaps the most famous and important locality for the Middle Triassic (Anisian/Ladinian) of North America, is truly outstanding. Aside from sheer beauty and spectacular preservation, the ammonoids and belemnites are cosied up to some spectacular well-preserved ichthyosaur remains.

Tozer's interest in our marine invert friends was their distribution. How and when did certain species migrate, cluster, evolve — and for those that were prolific, how could their occurrence — and therefore significance — aide in an assessment of plate and terrane movements that would help us to determine paleolatitudinal significance. I share a similar interest but not exclusive to our cephalopod fauna. The faunal collection of all of the invertebrates holds appeal.

This broader group held an interest for J.P. Smith who published on the marine fauna in the early 1900s based on his collecting in scree and outcrops of the West Humboldt Mountains, Nevada. He published his first monograph on North American Middle Triassic marine invertebrate fauna in 1914.

N. J. Silberling from the US Geological Survey originally published on these same Nevada outcrops in 1962 then teamed up with Tozer — bringing two delicious minds together to tease through the larger Triassic picture. Just prior and after Tozer's passing, Siberling went on to collaborate on papers with Haggart, Orchard and Paul Smith through to 2013. His work included nearly a dozen successive ammonite faunas, many of which were variants on previously described species. Both their works would inform what would become a lifelong piecing together of the Triassic puzzle for Tozer.

If one looks at the fauna and the type of sediment, the palaeogeography of the Triassic can be interpreted as follows: a tectonically calm west coast of the North American plate that bordered on an open sea; in the area far from the coast, a series of volcanic archipelagos delivered sediment to the adjacent basins. Some were lined or temporarily covered with coral wadding and carbonate banks. Deeper pools were in between. The islands were likely within 30 degrees of the triadic equator. They moved away from the coast up to about 5000 km from the forerunner of the East Pacific Ridge. The geographical situation west of the back was probably similar.

Jurassic and later generations of the crust from near the back have brought some of the islands to the North American plate; some likely to South America; others have drifted west, to Asia. There are indications that New Guinea, New Caledonia and New Zealand were at a northern latitude of 30 ° or more during the Triassic.

If you fancy a read, pick up a copy of Tozer's seminal publications: A Standard for Triassic Time (1967); and The Trias and Its Ammonoids: The Evolution of a Time Scale (1984). These are the culmination of over forty years of research. 

Fire and Ice: From the Arctic Archipelago to the Scorching Belly of Nevada. Fossil Huntress.

SOUTH CHILCOTIN MOUNTAINS PROVINCIAL PARK

The South Chilcotin Mountains Park has been home, hunting ground and trade route to local First Nations for thousands of years. The area falls within the territory of three Nations: Tsilhqot’in, St’at’imc, and Secwepemc. 

My interest in this part of the Chilcotin's is the geology and well-preserved fossil specimen it yields. To others, this region is a place to fish, hunt, collect berries and travel across as a trading route. While the area is now a protected park, it still sees a fair amount of recreational use.

Deer and mountain goats were hunted here for their meat and hides. Wool and horns were harvested from the region's goats for use as salmon spears. Special ceremonies were performed before hunting grizzly and black bear to honour their spirits and to thank them for the gift of their meat, fat and fur. Though common today, moose did not move into the area until about 1920. 

The skins of hoary marmots were used for robes and blankets and as trade goods. These were hunted in late summer or early fall after they had hibernated; the meat was smoked and the fat was particularly prized. Dash Hill, Cardtable Mountain, Eldorado Mountain, Teepee Mountain, and Graveyard Creek are known hunting sites.

South Chilcotin Mountains Park is situated in an area of complex geology that straddles the boundary between the southeast Coast Mountains and the Chilcotin Plateau. The geological history is one of the ancient ocean deposits, tectonic plate movement, faulting and mixing of rocks and layers of rocks, deposition of sedimentary rocks in shallow-marine basins, upwellings of granitic rocks and lava flows. Landscape features in South Chilcotin Mountains Park reflect the many complex geological formations that underlie it.

Sedimentary rocks are found in the heart of South Chilcotin Mountains Park through Upper Gun and Tyaughton Creeks and Relay and middle Tyaughton Creeks. They also form the height of land from Lorna Lake to Vic Lake in Big Creek Park.

Heidi Henderson and John Fam, VanPS

The serrated mountains in the Slim, Leckie and upper Gun creeks are underlain by granitic rocks that are a characteristic feature of the Coast Mountains. 

These granitic rocks are components of the continental margin magmatic arc related to subduction of oceanic rocks along the plate boundary to the west. This is a similar process to that still going on today and generating volcanic rocks such as Mt. Baker and Mt. St. Helens.

Volcanic rocks of Early to Middle Eocene (58 – 50 million years ago) age formed in several small volcanic centres scattered through the park. The most spectacular exposure is found at Mount Sheba, on the north side of Gun Creek.

The youngest rocks are part of the great lava flows of 16 to 1 million years ago that formed the extensive Chilcotin Plateau. Outlying remnants of these lava flows occur in the area of Teepee, Relay and Cardtable Mountains. On Relay Mountain the basalts are up to 350 metres thick.

Fossils are an important feature of South Chilcotin Mountains Park and demonstrate the marine origin of many of the sedimentary rocks. Well-preserved late Triassic marine fossils (ammonites and bivalves) are found in the Tyaughton Creek area. Lower and Middle Jurassic rocks in this same general area are also locally rich in fossils — mainly ammonites. The Relay Mountain Group is in part extremely rich in upper Jurassic and Lower Cretaceous fossils. Fossil-rich parts of the Relay Mountain Group are found around upper Relay Creek, Elbow Mountain and on the low bluffs northwest of Spruce Lake.

The faunal sequences based on ammonoids established for the Late Hettangian to Early Sinemurian interval in the Western Cordillera found here match-up rather nicely to those found in Nevada, USA.